applications and developments of sequence stratigraphy in latin america: synthesis of exploration...

8/20/2019 Applications and Developments of Sequence Stratigraphy in Latin America: Synthesis of Exploration and Development Experiences in the Sub-Andean Basins

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Copyright 2001, Society of Petroleum Engineers Inc.

This paper was prepared for presentation at the SPE Latin American and Caribbean PetroleumEngineering Conference held in Buenos Aires, Argentina, 25–28 March 2001.

This paper was selected for presentation by an SPE Program Committee following review of information contained in an abstract submitted by the author(s). Contents of the paper, aspresented, have not been reviewed by the Society of Petroleum Engineers and are subject tocorrection by the author(s). The material, as presented, does not necessarily reflect anyposition of the Society of Petroleum Engineers, its officers, or members. Papers presented atSPE meetings are subject to publication review by Editorial Committees of the Society of Petroleum Engineers. Electronic reproduction, distribution, or storage of any part of this paper for commercial purposes without the written consent of the Society of Petroleum Engineers isprohibited. Permission to reproduce in print is restricted to an abstract of not more than 300

words; illustrations may not be copied. The abstract must contain conspicuousacknowledgment of where and by whom the paper was presented. Write Librarian, SPE, P.O.Box 833836, Richardson, TX 75083-3836, U.S.A., f ax 01-972-952-9435.

AbstractApplying sequence stratigraphy concepts to the interpretationof petroleum and depositional systems constitutes afundamental approach for regional exploration and detaileddevelopment analysis. Distribution of reservoir, seal andsource rock represent primary parameters in the definition of

petroleum systems; description and weightiness of thesecomponents are critical in prospects; spatial distribution andarchitecture of rock facies are essential in appraisal anddevelopment of fields. Sequence stratigraphic concepts are a

proven powerful tool that gives the analyst a competitiveadvantage when defining the hydrocarbon potential from a

basin to a field scale project. It has proven particularly usefulwhen looking at old plays or mature basins in the search for upside or new plays. Forward modeling and prediction of

basin fill facies in data starved frontier areas has been another benefit from this technique. Application of the sequencestratigraphic tools is less obvious when dealing with terrestrialdeposits dominated basins.

Subandean basins present a variety of evaluationscenarios from the mature to the unexplored exploration/development settings. A few examples of Repsol-YPF assetsfrom the Eastern Venezuela basin; the Colombia Llanos basin;

Argentina. The Subandean basins of Latin America are theresult of a polyphase tectonic history that includes in mostcases a rift, back-arc and a foreland stages as a result of thetransition from a passive margin in the Lower Paleozoic to anactive margin in the Mesozoic and Cenozoic. A variety of source rocks and reservoirs are controlled by a combination of factors such as tectonics and eustacy giving a unique character to each basin fill in the Subandean dominion. Moderntechniques such as sequence stratigraphy allows the interpreter to give a renovated look to old plays and attempt theexploration of frontier areas. Is now a generalized procedureto interpret basin fill histories and their petroleum systems andapplications range from the reservoir to the basin scale. A fewexamples from Subandean basins are presented below todemonstrate the use and wide applications of the technique.

Sequence stratigraphy conceptsPeter Vail, Robert Mitchum and colleagues 1 in the classicalAAPG Memoir 26 first introduced sequence stratigraphy tothe world; even tough it was probably in use as an internalExxon tool since the early 70’s. The introduction of thisconcept revolutionized the geological thinking since it was astep forward from the facies and lithostratigraphic ideas of the60’s. The new idea helped the geologist to think in terms of seismic and created a strong link between the two disciplines.The concept of seismic markers being chronostratigraphiclines that represent sequence (or parasequences) boundaries

that could also be observed in well logs or outcrops made thegeological – geophysical world a single integrated powerfulentity.

The concepts behind sequence stratigraphy could beexplained trough the factors controlling the stratal patterns,that is: subsidence and eustacy. Subsidence is mainly aresponse to tectonic processes, such as faulting, thermal

SPE 69446

Applications and Developments of Sequence Stratigraphy in Latin America: Synthesisof Exploration and Development Experiences in the Sub-Andean BasinsM.A. Torres, R. Porta and I. Brisson, Repsol-YPF, Denver Technical Center.


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2 M.A. TORRES, R. PORTA, I. BRISSON SPE 69446

are explained under these assumptions by a series of cycles (or sequences) that are mainly a response to sea level change.Different type of stratal patterns and sequences are recognized

in different tectonic settings (foreland, extensional, passive or active margins, etc). A sequence is defined as a: “relativelyconformable succession of genetically related strata bounded

by unconformities or their correlative conformities” 1. Asequence is deposited between eustatic fall inflection points(or 3 rd order cycle: 0 .5 to 3 m. years) and is of a magnitude of the minimum interval that could be recognized on seismic.These cycles are believed to be controlled by glacio-eustacy 2.A sequence is further subdivide in “system tracts” which aredefined as a “linkage of contemporaneous depositionalsystems” 3 each associated with a specific segment of the of theeustatic curve. Sequence sets consist of a series of third order sequences with an average duration of 9-10 million years andare characterized by large eustatic falls.

Vail and colleagues 1 also introduced the concept of sea level curves at a global scale. The global sea level curvewas later modified by Haq and others 4 and presently is tieddirectly into the interpretation routine, particularly inexploration scenarios with poor coverage and frontier areas.

The global sea level curve idea is still controversial althoughhas demonstrated to be a very useful tool in some parts of theworld. A few examples are intended to present some cases inthis direction.

Venezuela: Eastern basinAppraisal and Development of the Quiamare FieldThe Middle Miocene Oficina Formation is the most important

producing unit at Quiamare Field. The Oficina Formation

consists of a succession of littoral to shallow marine deposits prograding to the N-NE. This oil-bearing parasequencesshows typical coarsening and thickening upward pattern,where coastal plain, foreshore, upper-, middle-lower-shorefaceand offshore facies were recognized. These shallow marine

parasequences shows a consistent facies change to the NEwith a paleo-coastline striking from N-NW to S-SE. Thisreservoir spatial architecture combined with the East-plungingnose-anticline of Quiamare structure creates the trap. Some

parasequences shows an internal facies shift, where coastal plain facies are flanked landward and basinward by shorefacedeposits; this discontinuity of facies tracts is interpreted asattached lowstand shoreline wedges or a forced regression.The importance of these reservoir wedges is reflected in thesandstone properties, controlling the primary porosity-

permeability distribution, which host the oil, and thesecondary fracture density which yield the oil consequently

Venezuela: Eastern basinExploration of the Talara DomeThe exploration of the external zone of the Serrania del

Interior Thrust Belt, Eastern Venezuela Basin, since the mid1980’s has resulted on the discovery of the supergiant ElFurrial field complex. The majority of these explorationefforts was and is focused on the Pirital thrust system locatedeast of the oblique ramp known as Urica fault. Thin-skinneddeformation is common with most oil and gas production fromanticlinal traps involving Oligocene and Cretaceous sandstonereservoirs. The Miocene section is composed by shaly faciesof Carapita formation that constitutes the super-seal.

In contrast, west of the Urica lateral ramp, there has been little exploration conducted in the Tala thrust system.There, a major stratigraphic change is present in the Lower Miocene, which is reflected by a facies change from slope-shaly facies of Carapita Formation to the sandy shallowmarine-deltaic facies of Capaya Formation. This sandy unit islimited at its base and top by flooding events dated at the

beginning and end of the Lower Miocene. Both floodingsurfaces acted as decollement planes during south vergentcompression, resulting in the development of a duplex

involving competent sandstones of Capaya Formation. TheCapaya sequences consist of coastal plain/ deltaic to fullymarine deposits that reflects deposition in low-relief rampsetting. Lowstand system tract containing incised and sheetlike fluvio-deltaic deposits or forced regressive shorelinewedges compose a typical sequence. Onlap terminations andfacies shift without facies transition marks the unconformitysequence boundaries. The transgressive systems tract iscomprised by backstepping of shallow marine sands and

offshore shales. Highstands shows similar facies arrangementthan transgressive system tracts in an agradational pattern. Themain reservoirs are associated to the lowstand sandy wedges,which are involved in the duplex structure that constitutes thetrap (Fig. 2 ).

In 1998 was drilled and completed the wildcat Tacatax-12 well that tested the play concept of Talara Dome provingoil in several Capaya sands, today the well is producing 4,400BOPD from two intervals and three appraisal wells weredrilled to delimitate and develop the discovery.

Colombia: Llanos basinCretaceous and Lower Tertiary stratigraphyand petroleum systemsDuring the Late Jurassic to Early Cretaceous back-arc rifting

phase, mainly marine sedimentation is recorded in the EasternCordillera and Llanos basin The final accretion of the


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SPE 69446 APPLICATIONS AND DEVELOPMENTS OF SEQUENCE STRATIGRAPHY IN LATIN AMERICA 3

accommodation space and important facies shift in shallowshelf to coastal environments.

Proven petroleum systems of the Llanos Foothills arerelated to the Santonian – Turonian global highstand shales of the Gacheta / La Luna / Plaeners Fms and the Tertiary sourcerocks of the Mirador (Eocene) and Carbonera (Oligocene)formations. Both petroleum systems are proven in fields likeCusiana-Cupiagua and Cano Limon with 2.7 and 1.5 BBO,respectively.

A sequence stratigraphic analysis of subsurfaceinformation helped determining the depositional history of theLlanos basin and understanding its exploration potential. The

present analysis is based on logs, seismic and biostratigraphicdata (Fig. 3).

It is interpreted that the cycle (sequence set 1) thatincludes the Fomeque/Villeta shales started in the Aptian at112 ma with a major marine transgression and a maximumflooding surface at the 103 – 98 ma interval 6. Seismic

backstepping geometries indicate transgressive conditions for most of the cycle and potential source rocks are expected inthis interval 7. The end of the cycle is interpreted at 94 ma. No

biostratigraphic or well data was available for this unit.

The next cycle (94 – 90 ma) (sequence set 2) beginswith a widespread forced regression at 94 ma in the fluvial-dominated to brackish marine (estuarine) Une sandstone. TheUne sandstone is considered a primary exploration target inthe Llanos basin for its excellent petrophysical conditions and

proximity to proven source rocks. Some controversy existswith regards to the Une nomenclature and some authors usethis name for the onlapping units of Aptian – Albian age(sequence set 1). The global Turonian - Cenomanian

transgression established tidal – marsh conditions starting aregional marine episode known as the Gacheta / La Lunashales. Only shallow marine to coastal facies in the Llanos

basin represents the global highstand of the Turonian andmore basinal, source rock quality facies are found to the westin the depocenter areas in the present Eastern Cordillera 8. Thecycle is capped by a forced regression deposited during a sealevel lowstand at 90 ma that initiated the next eustatic cycle(90 – 80 ma) (sequence set 3). Open marine conditions withnormal salinities (inner neritic) dominated the Santonian – Campanian sequence set in the Gacheta / La Luna / Plaenerstransgression. The persistence of the open marine conditionsduring this cycle is indicated by the presence of a localCretaceous maximum flooding in the Santonian. The marineto coastal Campanian Upper Guadalupe (85 – 80 masequences) prograding sandstones culminated the cycle.Guadalupe Fm provenance is from the eastern Guyana shield

progradational sequences and possibly erosion. This unit is a producing reservoir in fields like Cusiana and Cupiagua.

The following sequence set (sequence set 5) is

interpreted to correspond to the 68 – 56 ma cycle(Maastrichtian – Paleocene). Shallow marine with normalsalinity conditions were briefly reestablished and registered ina shaly interval below the Barco Fm. This Danian short-livedmarine episode (mfs at 65 ma) is truncated by the massiveBarco sandstone deposited in a costal environment in a

brackish tidal setting with fluvial influence indicating the persistence of the regressive conditions and an upward loss of accommodation space. Barco Fm provenance is also from theGuyana shield and is characterized by its high textural andcompositional maturity being composed by 95%quartzarenites. The Barco sandstone is a producing reservoir unit in Cusiana and Cupiagua fields. Finally, thissedimentation episode finishes with a major erosionalunconformity at the 56 ma sequence boundary. The erosionalunconformity represents a hiatus ranging from 56 to 42 ma(Ypresian - Lutetian). After this period of sediment by-pass,fluvial sandstones are deposited above the unconformity(Mirador Fm) followed by a marine transgression evidenced

by a thin shaly unit interpreted as belonging to the Barthonian(Late Middle Eocene) (sequence set 6). Some controversyexists regarding the age of the Mirador sandstone and other authors place this unit as upper Eocene 5,6. The Mirador sandstone is the main reservoir unit at Cusiana and Cupiaguafields. During the Early Oligocene a major marinetransgression flooded the entire basin known as the Carbonera8 unit. This flooding is interpreted as the beginning of the 39 – 30 ma sequence set (sequence set 7) under transgressive

conditions. Proven source rocks intervals were depositedduring these transgressive events in sequence sets 6 and 7.Tertiary oil families from the Caño Limon, Cusiana andCupiagua fields are correlated with these events. The 30 – 21ma cycle (sequence set 8) registered regressive conditions anddeltaic and fluvial units were deposited. This cycle includesthe Carbonera 1 to 7 units. By late Miocene times, after four episodes of Oligocene – Early Miocene northward deltaic

progradation the seaway finally closed. These deltaicsandstones represent important reservoir units in fields likeCaño Limon.

Peru: Marañon basinDepocenter exploration and Cretaceous stratigraphyThe Marañon basin is the Peruvian southern extension of thePutumayo-Oriente basins of Colombia and Ecuador. The basin


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between the producing areas and the rest of the basin and possibly aid in the identification of new plays.

Peru: Ucayali basinPaleozoic stratigraphy and petroleum systemsA synopsis of the complex stratigraphic history, driven by thedevelopment of an early Palaeozoic rifting phase,subsequently overprinted by numerous inversion phasesthroughout the Phanerozoic (low frequency cycles) and theinfluence of eustatic effects (higher frequency cycles), is

presented in Figure 5 . Although tectonics have been postulated to be controll ing the present day distribution of thesedimentary units, the variation in accommodation space hasdriven the successive alternation between starved andoverloaded basin condition that yield the development of themain reservoirs and source rocks present in the Ucayali basin.

The reservoir units are consistently deposited under conditions of a very restricted availability of accommodationspace, which has produced laterally continuous, sheet-like,sandstone bodies with good connectivity. This is observed assedimentation under conditions of normal regression (AmboGroup), forced regression (Green Sandstones, Ene Formation,

Chonta Formation) and even valley incision (MainiqueFormation and Vivian Formation).

The early Paleozoic Contaya Formation 10 and theCabanillas Group 10 are irregularly distributed within isolateddepocenters showing a “patchy” pattern, with verydiscontinuous, sometimes thick, wedge shaped deposits. Somesections, which are unconformable overlying the basement,measured in excess of 200 m, wedging out to the north. Onseismic this units show uplap termination onto the master

faults and a wedge geometry with at least one evident internalunconformity showing progressive rotation of the blocks.Described as shallow marine medium to coarse, light greenishgray, crossbedded, quartzose sandstones, this unit is assumedto be Early to Middle Devonian (Cabanillas Group) based onstratigraphic position and lithology. These sandstones areinterbedded with shales and are arranged in two major sedimentary cycles. General log response shows both of themdisplaying strong aggradational patterns with lessaccommodation space in the top cycle. This pattern suggeststhat the high rate of sediment supply and accommodationspace seem to be in pace for the whole unit, with highfrequency retrograding cycles that resemble a continentalstacking pattern. Devonian shales have proven to be suitablesource rocks 11 .

As a result of the lesser control of the pre-Eohercynian faults which only cut the oldest Carboniferous

therefore the cycles were assigned to the sequence set order.The Ambo Group is important as both a source rock andreservoir. The importance of Ambo shales as a source rock

for hydrocarbons has been proven by correlation with the producing Aguaytia Field and the giant Camisea gas andcondensate field 10,12 and by recent geochemical analyses of outcrop samples. Each cycle is capped by a thick delta frontsandy facies that prograde far into the basin whenaccommodation space becomes smaller. The sandstones aregenerally fair to good quality reservoirs. The age of thedescribed section has been bracketed as Tournaisian-Visean(Early Carboniferous) based on spores . A tendency of the

prograding lobes to drift towards the north is recognized andthe dispersion of the sandstones is very sensitive to the

position of the feeding channels. Seismic reveals a low angle prograding pattern.

The Late Carboniferous Tarma Group 10 is dividedinto a basal sandstone unit, informally denominated as GreenSandstones, and an upper section of thick limestones ( Fig. 5 ).The Tarma Group is dated as Middle Pennsylvanian based onforam content and is interpreted as a shallow marine/carbonateshelf deposit 13. The unit rests unconformable on the Early

Carboniferous Ambo Group. The parallelism in seismicreflections appears consistent with the Namurian hiatus

proposed in Ref.11 of eustatic origin 12. The Green Sandstoneshave been characterized as shoreline deposits, with astrandplain architecture, formed by the rapid accretion of

beach ridges towards the depocenter in a period of littleavailable accommodation space, corresponding to the Late

Namurian - Early Westphalian (early Middle Carboniferous)global sea level low. These sandstones constitute one of the

main reservoirs in the central Ucayali basin. The subsequentrise in sea level during the late Middle Carboniferous causedthe deposition of a transgressive sequence as evidenced by theintercalations of offshore shales and shelf carbonates of theuppermost Tarma Group. On seismic the Tarma Group ischaracterized by a series of (sub)parallel, high amplitudereflections.

The Upper Tarma Group (Late Carboniferous) andCopacabana Group (Early Permian) consist of a series of massive, stacked limestones with no recognizablediscontinuities. Based on the contrast of fossil fauna andregional evidence 13 between the two Groups, and on theabsence of the uppermost Pensylvanian fossil zone anunconformable relationship between the two groups is

proposed. The thick limestone section is a landmark in thestratigraphic evolution of the basin, recording the temporaryinhibition of clastic sediment supply


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6 M.A. TORRES, R. PORTA, I. BRISSON SPE 69446

at the base and top by unconformities (onlap basal/truncationand onlap fill/truncation respectively). The upper unconformity is assigned to the base of the Middle to Late

Cretaceous involving a hiatus of 120 million years minimumtime span (erosional plus non depositional hiatus). The EarlyPermian marine shales and shoreface clastics of the EneFormation constitute both source (high TOC-high quality) andreservoir rocks. The Mainique Formation comprises of threedifferent units: a lower sandy unit, that is interpreted to befluvial, a middle shaly unit that is considered marine, and anupper sandy unit described as continental fluvial deposits.Both the Lower and the Upper sections are considered goodquality reservoirs.

Argentina: Neuquen basinStratigraphy of Agrio, Chorreado and Troncoso InferiorThe Neuquen basin is located in the central western part of Argentina ( Fig. 6 ) and is the main producing basin in thecountry. Studied since the early 1900’s and producing for more than eighty years resulted in a strong stratigraphic,

paleontological and geochemical database. A very denseseismic 2D and 3D coverage provide reliable

seismostratigraphic interpretations.The Neuquen basin has been defined as an ensialic

back arc basin 14 that collected sediments from the latestTriassic to the recent. Despite of some important tectoniccontrol during the late Triassic and early Jurassic rifting phase,and some sporadic tectonic pulses during the Kimmeridgianand Valanginian, the pre Andean sedimentation was mainlydriven by eustatic control 15,16 producing a well developed thirdorder cyclicity.

The studied stratigraphic interval corresponds to theLate Cretaceous Upper Member of the Agrio Formation (LateHauterivian) and the Huitrin Formation (Barremian-Aptian) inthe southern part of the Mendoza and the northern part of the

Neuquen provinces. This interval shows a high frequencymodulation of generation of accommodation space that hascontrolled the development of a complex succession of reservoirs and seals 17.

The top of the Upper Agrio Formation is dated as113.5 ma, age that corresponded to the Intra-Barremianunconformity upon which the forced regression of theChorreado Member (base of Huitrin Fm) is registered. Asecond and more important unconformity separates the lastmember from the overlying Troncoso Inferior Member. Thisdiscontinuity is assigned to the Intra-Aptian unconformity(112 ma) that is responsible of the incision of the valley later filled with the fluvial/eolian deposits of Troncoso Inferior

Intra-Barremian unconformity. This geometric relationship isalso evident in the well logs correlations ( Fig. 6).

The overlying Chorreado Member has two sections, a

lower mixed clastic/carbonatic unit (Chorreado Inferior) andan upper evaporitic (Chorreado Superior) unit. The ChorreadoMember has a sigmoid profile thinning both basinward andlandward and shows a moderate high angle, oblique, seismicinternal reflection, with downlap to the center of the basin andtoplap and erosive truncation at he top ( Fig. 6) . The ChorreadoInferior was built by the alternation of: 1) epiclasticshoreface/offshore sediments, with SW-NE depositional strikethat correspond to sometimes detached and sometimesattached beach ridges that can develop a more or less extendedstrandplain complexes depending on the rate of progradation;and 2) limestones deposited in a temperate water ramp settingwith scarce and isolated biohermal buildups (Fig. 6). Theshoreface facies are good reservoirs that tested oil and gas inthe studied area. Occasionally, this facies are dissected bysmall channels that disperse the sediments further into the

basin developing lobe shaped sand bodies embedded by shalesthat has proven to be excellent reservoirs. The carbonatesfacies are good reservoirs only when fractured. Seven of these

lithological couplets (although the limestones are not always present) have been identified and interpreted as parasequencesets. Their stacking pattern shows a progressive losing of accommodation space. The set displays aggradational or evena slight backstepping at the base of the sequence (two first

parasequences sets) and finishes with a strong progradationalstacking pattern. Each parasequence set includes a shoreline

prograding deposit (interpreted as a high frequency forcedregression) and a carbonatic/shaly ramp that corresponds to a

deeper water level with an erosive transgressive surface in between conforming a fourth order complex sequence (in thesense of Van Wagoner et al 9).

The evaporitic Chorreado Superior Member is better developed to the north of this area and has been interpreted asan independent third order sequence 15. A strong drop of sealevel during the Aptian (112 ma) produced an incision of almost 100 meters that was subsequently filled during four successive stages ( Fig. 6 ). The lower stage (ChorreadoSuperior) corresponds to a hipersaline episode with onlappinggeometries in a restricted sea that progressed into a terrestrial

basin after the seaway closing. The Troncoso Inferior member is entirely terrestrial and has been divided into three units andinterpreted as a prograding wedge during a base levellowstand. The lower sandy/shaly section is restricted to thelowest part of the valley and has some relictic marineinfluence 18 The middle section is mainly sandy fluvial/eolian


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Argentina: Cuyo BasinExploration and development of Lower Rio BlancoThe Triassic Cuyo Basin is one of the most prolific

hydrocarbon producing basins in Argentina, with a cumulative production of one-billon barrels of oil, this basin host twogiant fields in a combined structural-stratigraphic trap settingVacas Muertas-Punta de las Bardas and Vizcacheras fields.

This Triassic basin develops two rifting phases RioMendoza-Las Cabras, and Potrerillos-Cacheuta-Rio Blanco,that evolves from overfilled to under-filled and overfilled -

balance-filled - overfilled lake cycle respectively, reflectingchanges in accommodation and climate progression. Severaldepositional sequences have been recognized and mappedthroughout the basin to accomplish the reservoir / source rock/seal architecture, on the basis of this detailed work andexploration program was delineated to investigate the Lower Rio Blanco sequences oil potential.

Depositional sequences of the Lower Rio Blancoembrace a deltaic – lacustrine parasequence set wherefluvio/deltaic lowstand wedge onlap the Cacheuta source rock.The lowstand wedge is covered by a transgressive restricted-lacustrine to fluvial deposits that comprise the seal. The

deltaic wedge in an updip termination constitutes the trapmechanism ( Fig. 7 ).

In 1992 an exploration well was drilled in thesouthernmost area of Punta de las Bardas Field to prove theconcept and tested 1566 BOPD of 30º API oil, the discoverywas developed with 11 wells.

AcknowledgementsThe authors gratefully acknowledge Repsol–YPF for

permission to publish this paper.References1. Vail, P. R., Mitchum, R. M. Jr., Todd, R.G., Widmier J. M.,

Thompson, S. III, Sangree, J. B., Bubb, J. N., and Hatleleid, W.G.: “Seismic stratigraphy and Global Changes of Sea Level”Seismic Stratigraphy-applications to hydrocarbon exploration,Payton, C. E. (ed.) AAPG Memoir 26 (1977) 49

2. Emery, D and Myers, K. J. (eds): Sequence StratigraphyBlackwell Science, Oxford, UK (1999)

3. Brown, L.F. and Fisher, W. L.: “Seismic stratigraphyinterpretation of depositional systems: examples from Brazil riftand pull-apart basins” Seismic Stratigraphy-applications tohydrocarbon exploration , Payton, C. E. (ed.) AAPG Memoir 26(1977) 213

4. Haq, B. U., Hardenbol, J. and Vail, P. R. : “Chronology of fluctuating sea-levels since the Triassic” Science, 235. 1153.

5. Cooper, M. A., Addison, F. T., Alvarez, R., Coral, M., Graham,d lh

6. Villamil, T.: “Campanian-Miocene tectonostratigraphy,depocenter evolution and basin development of Colombia andwestern Venezuela” Palaeo (1999) 153, 239.

7. Pindell, J.L and Tabbutt, K. D.: “Mesozoic-Cenozoic AndeanPaleogeography and Regional Controls on HydrocarbonSystems”, Tankard, Suarez and Welsik (eds.) Petroleum systemsof South America , AAPG Memoir 62 (1995) 101.

8. Villamil, T. and Arango, C.: “Integrated stratigraphy of LatestCenomanian and Early Turonian facies of Colombia”

Paleogeographic Evolution and Non-glacial Eustacy, NorthernSouth America , SEPM Special Publication No. 58 (1998), 129.

9. Van Wagoner, J.C., Mitchum, R. M., Campion, K. M. andRahmanian, V. D.: Siliciclastic Sequence Stratigraphy in Well

Logs, Cores, and Outcrops . AAPG Methods in Exploration

Series, No 7. (1990) 22.10. Perales Calderon F.: “Glosario y Tabla de Correlacion de lasUnidades estratigraficas del Peru” . I Congreso Latinoamericanode Geologia, Lima, Peru(1970)

11. Mathalone J. & M. Montoya: “Petroleum Geology of the Sub-Andean Basins of Peru”. Petroleum Basins of South America,

AAPG Memoir 62,(1995) 423.12. Schiefelbein C., H. Illich, J. Zumberge and Brown, S.: Peru Oil

Study. Regional Petroleum Geochemistry of Crude Oils from Peru. Geomark Research, Inc, Houston , Texas ( 1996)

13. Benavidez, V.: “Cuencas Paleozoicas en el Subandino Peruano”Exploracion Petrolera en las Cuencas Subandinas, SimposioBolivariano IV, Bogota, Colombia, Trabajo 34 (1991).

14. Mpodizis C. and Ramos, V.: “The Andes of Chile andArgentina”. Geology of the Andes and its relation to hydrocarbonand mineral resources Erickson G., M. Cañas Pinochet and J.Reinemund (eds.) Circum Pacific Council for Energy and MineralResources Earth Science Series, v 11 (1990) 59

15. Legarreta, L. and Gulisano, C.: “Análisis estratigráfico secuencialde la Cuenca Neuquina” Cuencas Sedimentarias ArgentinasChebli, G. and Spalletti, L. (eds.) ( 1989) 221

16. Legarreta, L. and Uliana, M. A.: “Jurassic-Cretaceous marineoscillations and geometry of back-arc basin fill, central ArgentineAndes”. Sedimentation, Tectonics and Eustacy Macdonald, G(ed.) (1991) 429

17. Brissón I., G. Olea, R. Varadé, N. Vitulli and Bolatti N.: “Controlde las Variaciones Recurrentes de Espacio de Acomodación enSistemas Depositacionales Mixtos del Cretácico Temprano”Cuenca Neuquina, Argentina. II Congreso Latinoamericano deSedimentología, Resúmenens, (2000) 53.

18. Legarreta, L.: “Análisis estratigráfico de la F. Huitrin (Cretácico

Inf.), Prov. de Mendoza” Tesis Doctoral, Universidad BuenosAires (1985)19. Gutiérrez Pleimling, A.: “Estratigrafía de la F. Huitrin: un estudio

puntual-Prov. del Neuquén” Boletin Informacion Petroleras YPF.September, (1991) 85

20. Mutti E., C. Gulisano and Legarreta, L.: “Anomalous SystemsTracts Stacking Patterns within Third Order DepositionalSequences (Jurassic-Cretaceous Back-Arc Neuquen Basin,


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Figure 3 ! Colombia: Llanos Basin

Cretaceous and Lower Tertiary stratigraphy and depositional environmentsLocation map

Lithostratigraphy Age SequenceStratigraphy

DepositionalEnvironments

Early Miocene

Oligocene

Middle Eocene

Campanian

Coniacian – Santonian

CenomanianTuronian

Paleocene

Maastrichtian

Carbonera

Mirador

Barco

Guaduas

Guadalupe

Plaeners

L.Guadalupe

UneGacheta / La Luna

30ma

56 – 42ma

60ma

68ma

80ma

90ma

94ma

39 ma

Tidal

Tidal, Marsh

Open Marine Neritic

Shallow Marine

Fluvial, Estuarine

Marine, Fluvial Infl.

Fluvial

Marine Neritic

Fluvial, Estuarine

Tidal Flats / Marsh

LST

LST

LST

LST

LST

KMFS

Shallow Marine

Coastal PlainDeltaic

Villeta / Fomeque Shallow Marine

112ma

Aptian - Albian

SequenceSets

7

6

5

4

3

21

8

+ Sea level -

Lithostratigraphy Age SequenceStratigraphy

DepositionalEnvironments

Early Miocene

Oligocene

Middle Eocene

Campanian

Coniacian – Santonian

CenomanianTuronian

Paleocene

Maastrichtian

Carbonera

Mirador

Barco

Guaduas

Guadalupe

Plaeners

L.Guadalupe

UneGacheta / La Luna

30ma

56 – 42ma

60ma

68ma

80ma

90ma

94ma

39 ma

Tidal

Tidal, Marsh

Open Marine Neritic

Shallow Marine

Fluvial, Estuarine

Marine, Fluvial Infl.

Fluvial

Marine Neritic

Fluvial, Estuarine

Tidal Flats / Marsh

LST

LST

LST

LST

LST

KMFS

Shallow Marine

Coastal PlainDeltaic

Villeta / Fomeque Shallow Marine

112ma

Aptian - Albian

SequenceSets

7

6

5

4

3

21

8

7

6

5

4

3

21

8

+ Sea level -

Llanos

basin

Llanos

basin


11/14

Regional East-West seismic line showing sequence sets geometries.Marañon Basin Cretaceous stratigraphy.

Regional seismic line.

Figure 4 ! Peru: Marañon Basin. Depocenter exploration and Cretaceous stratigraphy

M A H U A C A -1E A S T W E S TU N G U M A Y O -1 T IG R IL L O -1

6

PA L E O ZO IC

5

4

3

2

1

6 88 0

9 0

9 4

9 8

1 0 7

1 1 2

A G E SE Q U E N C E S E TS L IT H O

S T R A T IG R A P H Y SE A LE V E L

P A L E O C E N E

Y A H U A R A N G O

C A C H IYA C U

A G E ( M .A .)

V IV IA N

R IS E

A G U A C A L IE N TE

R A YA

C U S H A B AT AY

P O N A

LU P U N A

C A L IZ A

L O W E R C E TIC O

U P P E R C E T IC O

M A A S T R IC H T IA N

C A M P A N IA N

S A N T O N IA N

C O N IA C IA N

T U R O N I A N

C E N O M A N I A N

A L B IA N

6 8

5 8

8 0

9 0

9 4

9 8

1 0 7

1 0 3

11 2

7

6

5

4

3

2

1S E Q U E N C E S E T 1

E C U A D O R E C U A D O R

IquitosIquitos

Lim aLim a

T rujilloT rujillo

B O LIVIA B O L IV IA

C O LO M B IA C O LO M B IA

BR A SILBR A SIL

Océano PacíficoOcéano Pacífico

M arañonM arañon

E C U A D O R E C U A D O R

IquitosIquitos

Lim aLim a

T rujilloT rujillo

B O LIVIA B O L IV IA

C O LO M B IA C O LO M B IA

BR A SILBR A SIL

Océano PacíficoOcéano Pacífico

M arañonM arañon


12/14

Figure 5 ! Peru: Ucayali Basin. Paleozoic stratigraphy and petroleum systems

Chronostratigraphic chart

Location map

North-South Stratigraphic cross-section-Flattened to the top of Tarma Gp.

4 °

7 9° 7 5° 7 1°

0°

4°

12 °

16 °

8 °

1 2°

1 6°

75 ° 71 °79 °

8°

M O L L E N D

O B A S I N

100 0 100 200KM

SCALE

N

P R O G R E S OB A S I N

Z O R R IT

O S H IG

H

Talara

TA L A R AB A S I N

Piura

Bayovar

SANTIAGOBASIN

B A G U AB A S I N

L I M

N

A

S I

B A

LIMA

Chiclayo

Trujillo

Yurimaguas

Pucallpa

E NEB A S I N

UCAYALI BASIN

MADRE DE DIOS BASIN

MARAÑON BASIN Iquitos

BRAZIL

ECUADOR COLOMBIA

B O L I V I A

Ica

Cuzco

Moquegua

Tacna

Arequipa

Pto. Maldonado

M O Q U E G U A B A S I N

CHILE

L A N C O N E SB A S I N

Tumbes

S E C

H U

R A

B A S I N

T R U

J I L L O

B A S I N

S A L

A V E R R

Y B A

S I N

P I S C

O B A S I N

P

R

E

U

P

C

A

I

F

I C

O

C E

A N

A N D E A N

F R O N T

AN D E AN F R O N T

A T L

A N

T I

C O C E

A N

S O

U T H

R

E

A M

I

C A

P A

C I

F I C

A

E

O C

N

A N D E A

N F R O N T

T I T I C A C A B A S I N

H U A L L A G AB A S I N

c-

CATSINGARI SUR TARIZA CHIPANI

ANAQUIARI

PERRO

MASHANTONICHORINASHI

GATO

BASEMENT - pCDEL MARAÑON Gp.

CABANILLAS Gp. - EDv

AMBO Gp. - ECb

COPACABANA Gp. - EPm

COPACABANA Gp. - EPm

E N E F m .

- E P m

M AINIQ U E F m . - L

P m

ORIENTE Gp. - MLK

CHONTA Fm. - LK

VIVIAN Fm.

TARMA Gp. - LCbTARMA Gp. - LCb

Green sst.A M B O G p . - E C b

MF S

MF S- SB?

M F S -S B ?

MFS-SB?

T 1 S B - S SB

T 1 S B - S SB

SSB

SSB

SSB

SS B

MFS

MFS

T 1-SB? - BDS?

T 1-SB - SSB

T 1-SB

T2’s -SB?

S h i r a T h r u s t

D AT U M

LDv/ECb

LDv/ECb

LDv/ECb

TOUR/VIS

TOUR/VIS

ECb/FAMM.ECb/LDv

Pz/Rc

Pm/Tr

Pm/Tr

ECb/LDv

N S

* TOC: 0 .6-1 .46 /Ro: 1 .19

* TOC: 0 .5

* TOC: 0 .51

* TOC: 0 .8-1 .4 /Ro: 1 .03 * TOC: 0 .5-2 .27 /Ro: 1 .1

* TOC: 0 .23

* TOC: 0 .96 * TOC: 0 .32-0 .71

* TOC: 0.45

* TOC: 1 .33 /Ro:1 .15

* TOC: 0 .4-1 .74

* TOC: 10 .38 (HI :98) /Ro:1 .37

TOC: 1 .02-2 .18 *

TOC: 1 .15-1 .75 *

TOC: 3 .59 *

* TOC: 1 .1-1 .8 /Ro: 0 .77

* TOC: 1 .3-2 .2 /Ro: 0 .80

* TOC: 1 .29 /Ro: 0 .74

TOC: 0 .32

* TOC: 0 .79

* TOC: 0 .36

* TOC: 0 .31

* TOC: 0.29

* TOC: 0 .37

* TOC: 0 .85-2 .6 /Ro: 0 .85

* TOC: 1.61

* TOC: 2 .59 /Ro: 0 .83

* TOC: 0 .14

* TOC: 2 .77 (35 .63) /Ro:1 .15

* TOC: 0.29

* TOC: 0.17

4 3 8 M y T a c o n i a n

355 My Eo her cyni an

270 My Tardihercynian

2 2 0My Finihercynian

T e r t

i a r y

t r h u s

t


13/14

NW-SE Seismic Line-Flattened to the top of Troncoso Inferior.Location map.

Detailed stratigraphic column.

N-S Stratigraphic Cross sections-Flattened to the top of Troncoso Inferior.

Figure 6 ! Argentina: Neuquen Basin. Stratigraphy of Agrio, Chorreado and Troncoso Inferior

SENW

Tope TRONCOSO INF.

Tope AGRIO SUP.

PA

cf

bb

LimestonesShelf

ShalesLower shoreface/ Prodelta

Limestones/DolomitesCarbonate ramp

SandstonesFluvial non channelized

Sandstone/SiltstoneFluvial/Marsh

EvaporítesMarine hyp ersaline

SandstonesDunes

SandstonesShoreface/Delta front

Sandstone/Conglom.Fluvial channelized

Transgressive S .T.Non reservoir

Lower prograding wedgeNon reservoir

Upper prograding we dgeReservoir

Uncon.(11

2 M a ? . )

M. Troncoso Superior

M ( 1 13,5 a. ? )

E xag . Vert.: x 45

1º2,5 K m

F. Agrio (M. Superior)

M. Troncoso Inf erior

M. Chorreado Inferior M. ChorreadoSuperior

S N

TRO.SUP.

CHORRE ADOINFERIOR

CHO.SUP.

TRONCOSOINFERIOR

AGRIOSUP.

A ge

Upper Hauter ivian

Bar r emian

Aptian

Litho log y

Tr ansgr esive?

Upper Pr ogr adingWedge

Lower L.P.W.

TST

LST

HST

MS-3

MS-4

MS5

H-1

Lowstand(For cedRegr ession)

Highstand(Nor malRegr ession)

Fluvial

Evapor ites

FluvialBr aided

Car bonisticShelf

Mar .Hip.

Mar sh

Shelf

Top CHORREADO INF.


14/14

UPPER RIO BLANCO

RIO BLANCO FM

LRB C A C

H E U T A F

M

P O T R

E R I L L

O S F M

CABRAS FM

VILLAVICENCIO FM

A-1 B-2 C-3NORTH SOUTH

BARRANCAS FM

Figure 7 ! Argentina: Cuyo Basin. Exploration and Development of Lower Rio Blanco

Isopach Map

Lower Rio Blanco

Isopach MapPotrerillos +

Cachueta Fms.

StratigraphicCross-Section

Location map

applications and developments of sequence stratigraphy in latin america: synthesis of exploration...

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