exploration framework atlas series: volume i: · pdf filemaranon geanticline huallaga basin...

© Tectonic Analysis, Ltd., 2009

Tectonic Analysis Ltd.Chestnut House, Burton Park, Duncton,West Sussex, GU28 0LH, EnglandPhone/Fax: 44-1798-343517Web: http://www.tectonicanalysis.comEmail: [email protected]

Volume 2: Venezuela-TrinidadVolume 3: Ecuador-Peru-BoliviaVolume 4: Gulf of Mexico

TectonicAnalysis

Exploration FrameworkAtlas Series:

Volume I: Colombia

by

James Pindell & Lorcan Kennan

Tectonic Analysis, Ltd

http://www.tectonicanalysis.com

mailto:[email protected]

mailto:[email protected]; [email protected]



mailto:[email protected]

-83°

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Form more information see Appendix 1: Kennan & Pindell 2009. “Dextral shear, terrane accretion and basin for-mation in the Northern Andes: best explained by interaction with a Pacific-derived Caribbean Plate”. Geologicaland morphotectonic features referred to in the text. Map modified from Zamora and Litherland 1993;Schibbenhaus & Bellizzia 2001; Gómez et al. 2007, with SRTM30 digital relief. Map created with GMT softwareWessel, P. & Smith, W. H. F. 1991, Free software helps map and display data, EOS Transactions, AGU, 72, 441.

GEOLOGICAL AND MORPHOTECTONIC FEATURES OF THE NORTHERN ANDES

Exploration Framework Atlas Vol. 1 – Colombia © Tectonic Analysis Ltd. 2009

Fig. 15 (upper left). 46 Ma reconstruction of the circum-Caribbean region. Northward drift of the Caribbean(in the Indo-Atlantic hot spot frame) has stopped. Collision of Cuba with the Bahamas Platform terminatedthe opening of the Yucatán Basin and resulted in continued Caribbean-North America relative motion occur-ring on the Cayman Trough. The end of subduction beneath Chortís and Nicaragua Rise resulted in theirbeing incorporated into the Caribbean Plate. The southeastern Caribbean Plate advanced southeast towardthe central Venezuelan margin along the Lara transfer zone northeast of Lake Maracaibo. The southern partof the Panama Arc was accreting into the Ecuadorian forearc. Caribbean-South America motion rotatesalmost orthogonal to the Huancabamba-Palestina Fault Zone slowing the rate of northward terrane migra-tion in the Northern Andes.

Fig. 16 (mid left). 33 Ma reconstruction. The North America-Caribbean plate boundary is taking on the formof today‘s boundary system. South America-Caribbean motion is ESE-directed, resulting in overthrusting ofCaribbean terranes onto central and eastern Venezuela. Southeast dipping subduction beneath the north-ern Andes at the western South Caribbean Foldbelt was propagating eastward to the north of MaracaiboBlock. As the oblique collision progressed along Venezuela, continued convergence would necessarilytransfer to this eastward-propagating, south-dipping South Caribbean Foldbelt.

Fig. 17 (lower left). 19 Ma reconstruction. At this time, the tail of Chortís has moved far enough to the eastthat any N-S sinistral shear is not required, but W-E extension continues. Oblique collision along SouthAmerica has started to encompass the Serranía Oriental of Venezuela and Trinidad, and the South Caribbe-an foldbelt is now taking up most of the continued convergence to the west. The Margarita (or RoquesCanyon) transfer fault is feeding into the Urica transfer, thus allowing shortening to proceed in the SerraníaOriental. The Panama (PAN) Arc is choking the Western Cordillera-Sinú Trench and starts to escape to thenorthwest, relative to the Caribbean, bounded by northwest-trending sinistral faults and driving NW-directedthrusting in the western North Panama Fold Belt. Shortening at Colombia’s Eastern Cordillera and north-eastward migration of the Maracaibo Block is underway, adding in turn to the shortening at the South Carib-bean Foldbelt. The Galapagos Ridge was subducting somewhere along the Panama or Colombian margin.

Fig. 18 (lower middle). 10 Ma reconstruction. At this time, a fundamental shift in Caribbean motion withrespect to the Americas resulted in 085°-directed dextral shear dominating the SE Caribbean, and 070°-directed transpression dominating the northern Caribbean. The Cocos-Nazca Plate boundary jumped at thistime to the Panama Fracture Zone. The Panama Block has become partly coupled to the Nazca Plate,resulting in a Panama-Colombia collision that is presently occurring nearly twice as fast as Caribbean-SouthAmerica relative motion; thus, the northwest escape of the Panama slivers has ceased.

Fig. 19 (lower right). Present day plate boundary map of the Caribbean region, continuing the format usedin the preceding evolutionary figures, and showing the overall migration history of the central Caribbeanoceanic lithosphere in the Indo-Atlantic hot spot reference frame.

PLATE KINEMATICS – CIRCUM-CARIBBEAN FROM CAMPANIAN TO PRESENT

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30° 30°

NIC

PANMAR

HIS

AVE

YUC

CHI

GOM

CHO

GRAN

PR

Past position ofpresent coastlinein hotspot refer-ence frame

FarallonPlate

46 Ma

Palinspastic restorationof present coastline

Proto-CaribbeanInversion

Zone

EasternCordilleraAltiplano

SIU

1000 km

GalapagosHS today

S. Am.Plate

N. Am.Plate

FA/NA

FA/SA

CaribbeanPlate

15

1000 km

33 Ma

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0° 0°

10° 10°

20° 20°

30° 30°

CAY

PANMAR

HIS

AVE

YUC

CHI

GOM

CHO

GUA

PR

Altiplano

GalapagosHS today

CaribbeanPlate

FarallonPlate

N. Am.Plate

S. Am.Plate

FA/SA


Zone

FA/NA



16

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CocosPlate

CAY

PANMAR

HIS

AVE

YUC

CHI

GOM

CHO

SER

PR

c. 4 Ma afterbreakup

Altiplano

1000 km

19 Ma

GalapagosHS today

S. Am.Plate


NZ/SA

N. Am.Plate


NazcaPlate


Zone

CaribbeanPlate

17

1000 km

10 Ma

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20° 20°

30° 30°

CocosPlate

CAY

PAN MAR

HIS

AVE

YUC

CHI

GOM

CHO

SER

PR

Restored positionof present borders

gray and black arrows arepre- and post-10 Ma azi-muths of Caribbean/SouthAmerica relative motion

GalapagosHS today

NazcaPlate

NZ/SA



N. Am.Plate

AltiplanoS. Am.Plate

CaribbeanPlate

18

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-10° -10°

0° 0°

10° 10°

20° 20°

30° 30°

1000 km

0 Ma

NazcaRidge

CocosPlate

CocosRidge

CarnegieRidge

Mid-AtlanticRidge

AltiplanoSubandes

AbancayDeflection

HuancabambaDeflection

CentralAndes

NorthernAndes

Fifteen-Twenty

Yucatán

Gulf of Mexico

125

100

84

7156

46331910 0

Motion of Caribbean inIndo-Atlantic hotspot

reference frame

Galapagoshot spot

N. Am.Plate

S. Am.PlateNazca

Plate

CaribbeanPlate

Chortís

19

Vector Triangles defining stages of relative motionbetween NA, SA, and CA, calculated at 11°N, 75°W.

N

0 5 0 100

km

74 Ma

33 Ma

59 Ma

25 Ma

19 Ma

12 Ma

10 Ma

0 Ma

9.6 - 0 Ma triangle

19.1 - 12 Ma triangle

12 - 9.6 Ma triangle

25 - 19.1 Ma triangle

33 - 25 Ma triangle

46 - 33 Ma triangle

59 - 46 Ma triangle

84 - 74 Ma triangle

74 - 59 Ma triangle

These pointshave poor control

Flow path of NArelative to SA,(Müller, 1993) 89 Ma

onset of Cayman Troughopening (160 km after ~50 Ma)

65 km

140 km

Note: Total CA/NA during Cayman Trough stage is c.1150 km, 20 km of which occurred along the SE flank.

CA relative to SA

NA relative to SA

CA relative to NA

46 Ma

221 km, 23mm/yr

AndeanOrogenybegins

Note: Period of Antilles-Bahamascollision: Cayman Trough takes over fromAntillean Trench as the main zone of NorthAmerica-Caribbean relative motion.

•

•

•

•

••

•

•

•

•

Fig. 20. Derivation of South America - Caribbean motion since Late Cretaceous.SoAm-NoAm (green) is based on Atlantic magnetic data, Carib-NoAm (red) isbased on Cayman Trough data (since Eocene) and northern Caribbean geology,Carib-SoAm (blue) is based on vector triangle closure. Note that NoAm-SoAmconvergence provides strong N-S component for Carib-SoAm.

Fig. 21. Bar graph of Caribbean-SoAm velocity since Late Cretaceous (blue issmoothed). West drift of SoAm dominates relative motion. Note Early Paleogenerapid motion, culminating in “Eocene Orogeny”; Andean Orogeny may relate tochange to more head-on subduction beneath Colombia, combined with a slow-ing of Caribbean rollback at Colombian trench and the presence of Panama atmuch of trench choking the subduction zone.

090

252015105

50607080 010203040Time to present

303540

030°

035°

045°

080°

090°090°115°

110°

mm

/yr,

orkm

/Ma

AZIMUTH(CA/SA)

This spike seen when hotspot motiondata is sampled more closely


Page 7

CRETACEOUS STRATIGRAPHY BY REGIONFig. 42. Compilation of Cretaceous-Early Paleocene stratigraphic units by region.

BER

VAL

HAU

BAR

APT

ALB

CEN

TUR

CON

SAN

CAM

MAA

CO

LON

FO

RM

AT

ION

CO

LON

MU

DS

TO

NE

SO

CU

YM

EM

BE

R

LALU

NA

FO

RM

AT

ION

CO

GO

LLO

GR

OU

P

Martínez,1989

UM

IRF

OR

MA

TIO

N

LALU

NA

FO

RM

AT

ION

GALEMBOMEMBER

SALADA

PU

JAM

AM

EM

BE

R

EL SALTOFORMATION

SIMITIFORMATION

TABLAZOFM.

PAJAFM.

ROSA-BLANCA

FM.

TAMBORFORMATION

GR

UP

OC

AL

IZO

BA

SA

L

?

Julivert,1961

LUTITAS DEMACANAL

?

AR

EN

ISC

AS

DE

LA

SJU

NT

AS

APON FM.

UN

EO

RA

GU

AR

DIE

NT

EF

OR

MA

TIO

N

CH

IPA

QU

EF

OR

MA

TIO

N

LA LUNAFORMATION

LOS PINOSFORMATION

GUADUASFORMATION

Etayo-S.,1985

Etayo-S., 1979

?TIERNA FM.

ROSA-BLANCA

FORMATION

?ARCABUCOFORMATION

PA

JAF

OR

MA

TIO

N

LUTITASNEGRAS

INF.

AR

CIL

LOLI

TA

SA

BIG

AR

RA

DA

S

LOWERSAN GILS

AN

GIL

GR

OU

P

UPPERSAN GIL

FM.

CHURUVITAFORMATION

SAN RAFAELFM.

CONEJO FM.

CUCAITAMEMBER

LIDITASUPERIOR

GUADUASFORMATION

?

GU

AD

ALU

PE

GR

OU

P

UP. LIDITA

L. LIDITA

GUADUASFORMATION

?

LABORAND

TIERNAFMS.

VIL

LET

AG

RO

UP

LAN

AV

ET

AF

OR

MA

TIO

N

BEJUCALMBR.

EL DIAMANTE

PIN

ZA

IMA

-UT

ICA

FM

(SA

RM

IEN

TO

,198

9);

UP

PE

RC

AQ

UE

ZA

(VIL

LAM

IL,1

992)

FRONTERA

HILO FM.

SOCOTA

TRINCHE-RAS

?

LOWERSS.

TETUANLIMESTONE

BAMBUCA SH.

CABALLOSL

MU

VIL

LE

TA

FO

RM

AT

ION

LOWERCHERT

EL COBRESS.

BUSCAVIDAS

GUADUASFM.

MONSERRATEFM.

Barrio &Coffield,

1992.

2ND ORTEGA LS.

2ND ORTEGASS.

1ST ORTEGASS.

OLINI SH.

TETUANLS.

BAMBUCASH

LA LUNA LS.

AICOSHALE

UP. CHERT

LOWERCHERT

CA

BA

LL

OS

GUADUAS

MONSERRATEFM.

UP. CHERT

VIL

LE

TA

FO

RM

AT

ION

Allen,1989;

Texas,1962

PLAENERS

VIL

LE

TA

FO

RM

AT

ION LOWER

CHERT

CABALLOSFM.

MO

NS

ER

RA

TE

FM

.

GUADUAS

Beltranand Gallo,

1979.

CIMARRONA

LATABLA

NIVEL DE LUTITASY ARENAS

UP LIDITA

LO LIDITA

OL

INIG

RO

UP

LUTITAS

LOMAGORDA

FORMATION

HONDITAFORMATION

Porta,1965

VIL

LE

TA

GR

OU

P

LOWERCABALLOS

UPPERCABALLOS

CA

BA

LL

OS

FM

HILO FM.

HO

ND

ITA

OR

LA

FR

ON

TE

RA

FM

.

LO CHERT

UP CHERT

OL

INIG

R.

GUADUAS

GUADALUPEFORMATION

?

NO

TS

TU

DIE

D

Miller,1972

FOMEQUEFORMATION

CAQUEZAGROUP

FRONTERA

L. CHERT

U. CHERT

GUADUAS

GU

AD

AL

UP

EG

AC

HE

TA

GR

OU

P

CHIPAQUE

UNE

UBAQUEFM.

PAL

?

GU

AD

AL

UP

EG

R.

GA

CH

ET

A

Villamil,1994

?

VIL

LE

TA

GR

.

RUMIYACOR

ION

EG

RO

MO

LIN

AF

OR

MA

TIO

N

CERAJON/STA. CRUZ

FORMATION

CR

ET

AC

EO

US

PR

ES

ER

VE

DIN

SC

AT

TE

RE

DP

OR

TIO

NS

OF

TH

EB

AS

IN

LOWER SOCHA CACHO

UPPER SOCHA (Los Cuervos in foothills)

?

LISAMA

CR

ET

AC

EO

US

CABALLOS

???

?

Stage Cesar-Rancheria

MiddleMag.Valley

S.N. delCocuy

Villa deLeiva

Bogotá-Apulo

EasternBogotá Upper Magdalena Valley Llanos Putumayo

LowerMag.Valley

BARCO-CUERVOS

CRETACEOUS STRATIGRAPHIC COLUMNS

NO

TM

EN

TIO

NE

D

Hatchured areasrepresent timenot recognised.


Page 16

-82°

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-76°

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-75°

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-73°

-72°

-72°

-71°

-71°

-70°

-70°

0° 0°

1° 1°

2° 2°

3° 3°

4° 4°

5° 5°

6° 6°

7° 7°

8° 8°

9° 9°

10° 10°

11° 11°

12° 12°

13° 13°

14° 14°

15° 15°

71.0°72.0°

73.0°

74.0°

75.0°

76.0°

77.0°

78.0°

1.0°

2.0°

3.0°

4.0°

5.0°

6.0°

7.0°

8.0°

9.0°

10.0°

11.0°

12.0°

Venezuela

Colombia

Mocoa

Florencia

Gigante

Neiva

Popayán

Villavicencio

Chaparral

Bogotá

Honda

La Paz

Tunja Yopal

BucaramangaSan Cristóbal

Valledupar

Santa Marta

Riohacha

Maracaibo

Dina field

Infantas field

Orito field

Apiay field

Cusiana field

Caño Limón field

Tibúfield

Ibagué

Cucutá

Pasto

Paz del Río

El Banco

Mag

dalen

a River

La Luna

Aguardiente

Churuvita

K-7informal

Villeta

Villeta

Upper Cogollo

Guayacan

Tocuycalcareoussandstones

Unnamed calcareoussandstones. "Calizade Mermetti"

then a transgressive surface

stron

g regres

sion

(sequ

ence

boun

dary)

,lo

wst

and

follo

wed

bya

still

stan

dan

d slow

trans

gressi

on

(prog

rading

comple

x)

approximate western limitof pre-Mesozoic crust

approximate western limitof autochthonous basementwhich was not thermallyaffected in Late Cretaceous

Maracaibo Fracture Zone

ColombianMarginalSeaway

Proto-CaribbeanSeaway

Tahami

ABCIslands

Grenada Basin(closed untilLate Maast.)

Villade Cura

Tobago

Margarita

Caribbean-SouthAmerica motion

c. 27 km/Ma

AvesRidge

East-dipping subduction beneathfuture Cauca-Almaguer (orRomeral) Fault will result inaccretion of Caribbean crust slicesto form Western Cordillera

Arquia-Quebradagrande

Terrane

Earliest AntioquiaBatholith, AltavistaStock (c. 95 Ma)

No strat. record of thisage on Antioquia Terrane

No known facies of this age (because of non-deposition,erosion, thrusting and metamorphism, etc.)

Coastal fringe (deltas, estuaries, beaches, lagoons etc.)

Shallow (inner) shelf (+/- carbonate)

Deep Sea

Deeper (outer) shelf

V Primary axis of magmatic arc (subduction-related)

Condensed sections

Cherts

Fluvial/non-marine, inferred coastal onlap

Halite dominated salt basin

Granitoids (incipient arc, Caribbean subduction)

Mixed evaporite, shallow marine fringing sabkhas

Western limit ofCretaceous control

Non-reef

Reefal

200 km

Palinspastically relocated geographic boundaries(coastlines, continental margins, national borders)

Present geographic boundaries of all types

Palinspastically relocated latitude/longitude lines

Palinspastically relocated locations of cities/fields

Palinspastically relocated traces of key present-day rivers

Paleostructure:Thrust/trench: Rift/normal fault:

Strike-slip, left lateral: right lateral:

Transpression: Transtension:

Fig. 52. Late Cenomanian Paleogeography©Tectonic Analysis 2008

LATE CENOMANIAN PALEOGEOGRAPHYThis map (Fig. 52) is based on a regional reconstruction for c. 96 Ma (see Figs 10, 11). The leadingedge of the Caribbean Plate has almost reached northern Colombia, by remains offshore to the west,reflecting ongoing separation between the Americas. By this time, closure of the Andean back-arcbasin was more or less complete, and subduction of the leading edge of Caribbean crust beneathAntioquia was well-established. The earliest phases of plutonism in the Antioquia Batholith andAltavista Stock cut across previously emplaced thrust slices of mafic and ultramafic rock. The formerTrans-American Arc (part of all of the Quebradagrande Complex) lies west of the incipient AntioquiaArc, and Western Cordillera basalts of Caribbean origin will be accreted to its western side during theLate Cretaceous. We suspect that tears developeda t this time in both the South American plate (alongthe line of the former continent-ocean boundary northwest of Antioquia) and the Caribbean Plate(along the transform which separated over-riding and subducting portions of the plate). These tearsallowed synchronous subduction of former Colombian Marginal Seaway oceanic crust underneathrelatively more buoyant Caribbean crust northwest of Antioquia and subduction of Caribbean crustbeneath relatively more buoyant South American crust at and south of Antioquia. The tears, the jux-taposition of hot and cold lithosphere and asthenosphere across them, and the melting of the edges ofthe newly-torn plates contributed to Cenomanian–Turonian magmtism such as the Antioquia Batho-lith and Aruba Batholith that are not easily assigned to conventional subduction-related arc origins.

Regionally widespread but volumetrically small mafic to intermediate intrusions and lava flows arefound throughout the Eastern Cordillera of Colombia (Vasquez & Altenberger 2005) and also in theOriente Basin of Ecuador (Barragán & Baby 2004), with K-Ar or Ar-Ar ages ranging from 120–136Ma (Colombia), 101–106 Ma (Ecuador), 95–96 Ma (Colombia, this map), 91–92 Ma (Ecuador), 82Ma (Ecuador) and 74 Ma. All have alkaline, non-sudbduction-related geochemical character andhave been interpreted to represent either magmatism associated with ongoing rifting or plume forma-tion. Especially for later examples we prefer the latter explanation because of the lack of other explic-it evidence of active faulting or dramatic thickness changes in Late Cretaceous strata across faults.Other possible plume-related magmas of Cretaceous age are known from Bolivia, western Brazil andas far as the Gulf of Mexico. Even the younger c. 100 Ma rifting event identified by Sarmiento et al.(2006) may be called into doubt given the numerous stratigraphic and paleontologic problems wehave identified in the Eastern Cordillera and given that many authors lift stratigraphic names and ageassignments from incomplete literature than does not always recognize the sequence stratigraphiccomplexities of the area.

The Late Cenomanian in Colombia and western Venezuela is characterized stratigraphically by a rel-atively abrupt basinward shift in facies, which records a significant drop in relative sea level. Thisshift in facies can be identified in the Upper Magdalena Valley as a laterally-discontinuous sandstonepackage of about 3 meters in thickness, interpreted as the lowstand systems tract associated with theunderlying sequence boundary. In other areas of Colombia this level is often described as a regionallydeposited limestone, but it is actually a calcareous sandstone in some regions and a shallow-waterlimestone in others. This unit has been called “Caliza de Exogyra Mermetti” by many authors, andhas an abundant and characteristic fossil content including the bivalve Exogyra squamata.

Sandstone packages prograded to regions of the Upper Magdalena Valley after 6 Ma of shale deposi-tion with facies similar to the older Caballos Formation. These sandstones or sandy limestones havenot been much considered or tested as reservoirs but their lateral discontinuity and their regionalcharacter suggest that they could serve as adequate and predictable reservoirs, especially for strati-graphic traps, as they are underlain and overlain by shaly source rocks.

The top of the latest Cenomanian lowstand deposits was slowly transgressed and then rapidly cov-ered by distal, offshore, hemipelagic limestones and highly calcareous shales of the Early Turoniantransgression (following map).

Corona gabbro-tonalite shallowintrusions

V/G


Page 25

?

?

-82°

-82°

-81°

-81°

-80°

-80°

-79°

-79°

-78°

-78°

-77°

-77°

-76°

-76°

-75°

-75°

-74°

-74°

-73°

-73°

-72°

-72°

-71°

-71°

-70°

-70°

0° 0°

1° 1°

2° 2°

3° 3°

4° 4°

5° 5°

6° 6°

7° 7°

8° 8°

9° 9°

10° 10°

11° 11°

12° 12°

13° 13°

14° 14°

15° 15°

V

V

V

Mocoa

Florencia

Gigante

Neiva

Popayán

Cali

Villavicencio

Chaparral

Bogotá

Honda

La Paz

TunjaYopalManizales

Medellín

Bucaramanga San Cristóbal

El Banco

Valledupar

Santa Marta

Riohacha

Maracaibo

Dina field

Infantas field

Orito field

Apiay field

Cusiana field

Caño Limón field

Tibú field

Ibagué

Cucutá

Pasto

Paz del Río

Santos111 well

9.0°

10.0°

9.0°

75.0°

7.0°

5.0°

10.0°

8.0°

Nazareth FmMacarao Fm

upper Mirador Fm,lakeside braidplain delta

Ciénaga de Oro Fm,mainly deltaic,

starting to onlap theLower Mag.

Esmeraldas Fm,mostly lake deposits

Guachinte Fm

Limit ofMirador

Arauca Mbr ofGuafita Fm,

onlapping E-ward

Mirador Fmsensu Caño Limón,onlapping E-ward

Caribbean Plate

"Eocene Unconformity" sensuMaracaibo is likely due to isostatic

rebound of Oca Fault footwall duringtranstension along Oca Fault, possibly

linked to deep breaking of the olderMaracaibo Fracture Zone

Upper Carbonera Fm,southward? flowing

Central Cordillera waskept elevated by Carib-

bean underthrusting

Siamana Fm

Carbonera Fm

Triple junction migration transfers north toBuenaventura Fault. Cauca Valley deposition will

occur at first above the growing accretionary prism,and then (Miocene) between areas of uplift in the

Central Cordillera and the Western Cordilleraaccretionary prism.

FarallonPlate

Lara Nappes fullyemplaced at this time

west end ofGuarico Basin

foredeep, ahead ofLara Nappes

?

?

Lake EsmeraldasLa Paz "II" Fm,mostly fluvial,

representing theonlapping fringe of

lake system

La Paz"II" Fm

Vaupes Arch

offshore lake shales w/condensed Fe-oolite beds,

underlain by Picacho IIbasal onlapping sands

Lower Concentración Fm

Regadera Fm

?

?

?

Chicoral andPotrerillo Fms

"Fusagasugá" Fm

Olini Group issource of chert inGualanday Gp.

UndifferentiatedPanama Arc

In Upper Mag, Chicoral Fm alluvial fansintertongue with Potrerillo Fm mudflats

and/or overbank deposits within the"Gualanday" foredeep basin, whichformed due to intermittent thrusting

at the Chusma and related thrustsalong E flank of the Central Cordillera.

Drainage dividebetween northern

and southern basins?

“Rom

eral L

ineam

ent”

Sinú

Tren

ch

Jacin

to

Belt

San

Coals inCauca Valley

Leading edge ofCaribbean slab

at 33 Ma

Southern Cauca Valley probablyflowed south at first, due to

underthrusting of Caribbean slabin this region

Orteguaza Fm

basal conglomeratein Mosquera Fm

Chus

ma Fault

Zone

Chicoral andPotrerillo Fms

Cicuco

SanLucas

Dificil

Segovia

Sta. Marta

Oca fault

Falcón Basinreleasing bend

Chronostratigraphiccross-section III

Chronostratigraphiccross-section I

Chronostratigraphiccross-section II

San Mateo Fmfanglomerates

Buen

aven

tura

Faul

t

PiñonTerrane

Hua

ncab

amba

Faul

t

Lateral ramp north of Guajiramimics trend of underlyingMaracaibo Transform

Arquia-Quebradagrande

Terrane

Margarita Fault

Cau

ca-A

lmag

uerF

ault

Zone

Silv

ia-P

ijao

Faul

tZon

e

Caribbean-SouthAmerica motion

c. 18 km/Ma

Antioquia in finalposition wrt MMV

Panama

Montaigne MarlsABC

Islands

Bonaire Basin

ChocóTerrane

South Caribbean Foldbelt

Villade Cura

outflowfrom lake?

No known facies of this age (because of non-deposition,erosion, thrusting and metamorphism, etc.)

Primarily braided rivers

Meandering rivers, overbank usually dry (vegetated)

Large, long-lved lakes

Meandering rivers, overbank permanently flooded(“wet overbank”, ie.e lakes, swamps)

V Primary axis of magmatic arc (subduction-related)

Conglomeratic fans(alluv. and marine)Sandy fans (marine)

Coastal fringe (deltas, estuaries, beaches, lagoons etc.)

Primarily alluvial fans

Shallow (inner) shelf

Deep Sea

Deeper (outer) shelf

Accreted Caribbean oceanic plateau basaltsVV

A

FB

FD

FW

200 kmFig. 77. Latest Eocene–Earliest Oligocene Paleogeography©Tectonic Analysis 2008

Palinspastically relocated geographic boundaries(coastlines, continental margins, national borders)

Present geographic boundaries of all types

Palinspastically relocated latitude/longitude lines

Palinspastically relocated locations of cities/fields

Palinspastically relocated traces of key rivers

Paleostructure:Thrust/trench: Rift/normal fault:

Strike-slip, left lateral: right lateral:

Transpression: Transtension:

A

FB

FD or FB

FW

A

A

A

FW

FW

LATE EOCENE TO EARLIEST OLIGOCENE PALEOGEOGRAPHYTo the south at this time, in the Upper Magdalena Basin, this style of gentle subsidence, progressiveonlap of Central Cordillera, and interior lacustrine deposition is not seen, even though it is clear thatthe Upper Magdalena Basin directly overlay the southern edge of the Caribbean Plate for LateEocene-Late Oligocene time. Instead, syn-orogenic deposition is the rule as shown by the conglomer-ates (alluvial fans; Chicoral, Regedera II, San Juan de Ríoseco, Fusafugasa, and Doima formations),sandstones (fluvial systems; Gualanday, Potrerillo formations), and mudstones (overbank depositsand possible sabkhas; Potrerillo Formation) of the ?Late Eocene to Early Miocene Gualanday Group.In the Late Eocene, the change to such deposition was geographically transitional from north to south,as shown by the “less proximal” Regedera II Formation in the southernmost Sabana, which is itselfoverlain by the intermittently lacustrine deposits (southern portion of Lake Esmeraldas) of the lower,Late Eocene-Early Oligocene, part of the Usme Formation. The facies of the Gualanday Group of theUpper Magdalena Basin indicate fairly continuous or repeated uplift and erosion of Cretaceous (e.g.Olini cherts), Jurassic, and basement rocks from the Central Cordillera to the west. Alluvial fans sheddetritus eastward into adjacent fluvial systems with broad, muddy alluvial plains. The associationcomprised a respectable foredeep basin, as the Gualanday Group as a whole can reach up to 3000meters in thickness. Syn-depositional tectonic loading in the west is clear. The Chusma Thrust Beltis a collection of thrusts on the west side of the Upper Magdalena Valley and is at least partiallyresponsible for the loading of the foredeep basin. These thrusts carry basement over the westernmostGualanday Group and also cut it in many places, almost always with eastward vergence. TheChicoral and Potrerillo Formations are more tectonised than is the younger (Early Miocene) DoimaFormation, suggesting that syn-depositional thrusting continued during the Late Eocene, Oligocene,and Early Miocene.

8°

83°

9°

10°

7°

6°

11°

82°84°85°86°

V

V

V

VV

200m

200m

Limón Basin

Pana

ma

Frac

ture

Zone

Cocos

Ridge

Caribbean SeaNic.

C.R

.Pa

n

C.R.

Middle

Trench

America

V

Limón Basin-Upper Magdalena Basin Analogue

Hess Escarpment

Cocos Plate

Fig. 78. The Limón Basin of CostaRica provides an excellent analoguefor our interpretation of the tectonicsof the Upper Magdalena Basin forEocene through Miocene times. InCosta Rica, subduction of thebuoyant Cocos Ridge causes 4 localdevelopments: (1) gap in arcvolcanism, (2) relatively hightopography in the arc, (3) elevation ofthe forearc with the coast very nearthe trench, and (4) strongbackthrusting of the arc within andover the "multi-piggy back" LimónBasin. In the Paleogene Upper MagValley, subduction of the eastwardcontinuation of the Panama Ridgeshould have produced the sameeffects. The geological record bearsthis out, namely the development ofthe mainly east-vergent ChusmaThrust Belt and syntectonicsedimentation within the piggy-backGualanday foredeep basin.


Page 40

Cauca-Patía

Time Setting/Stage Source Reservoir SealTraps Maturation Migration history

Timing

Basin:

Stratigraphy

I, II, III, type org. matter. F, fault. S, strat. C, combo.InferredKnown

Mostly marineMostly non-marine

L

M

E

L

L

L

E

E

E

E

E

L

L

M

Jurassic

LowerCret.

UpperCret.

Paleo-cene

Eo

cen

e

Oligo-cene

Mio

cen

e

Pliocene

Quat-ernary

Arc flare up

Short-lived arc flare up

Galeón

Esmita Congl.

? ? ? ?Uplift of WesternCordillera

Folding within basin

Esmita sand

Marginal marine

Mosquera

Peña Morada?

Chapungo

Uplift of CentralCordillera (Eocene un-conformity develops)with turbidites andconglomerates inwestern prism

Western Cordilleraeroded and coveredby coastal sediments

Ocean floor shale andlimestone accreted inPaleocene

Basement of accretedocean floor fragments

III, rare II1-4%

II,1-4%(?oilprone?)

III ± II4-70%

(coals)Note:Mataceaoil seepis fromtype IIIkerogen

2% 2°φ

2% 2°φ

14% 1°φ(this is bestreservoir)

<9% 1°φ2° φ (lsts)

C? (slight u/cat top Mosquera)

S (variable coast-fluvial facies inMosquera +Esmita Fmsgive wide varietyof strat. traps)

S

S

S (angular u/c atbase Galeón)

S

Maturation modelling indicates thatmain pulse of migration from lateCretaceous source (combinedstratigraphic or structural burial)and Mosquera/Esmita sources (thesecan only mature by thrust burial)must occur at about the same timeas the formation of the majorstructural traps

(goodsealingclays)

No possibility for burial-drivenmaturation and migration

(?gasprone?)

Possible structure-driven expulsionduring formation of Paleocene-Eocene accretionary prism but littlelikelihood of preservation in viablereservoirs.

Tmax of450-550

Ro 0.7-3.4%Tmax of410-466

Ro 0.3-2.5%Tmax of410-455

May be transitional

"Eocene"unconformity

TectonicAnalysis

Fig. 107

BASIN EVENT CHART – CAUCA-PATIA BASIN


Page 69

-80°

-80°

-79°

-79°

-78°

-78°

-77°

-77°

-76°

-76°

-75°

-75°

-74°

-74°

-73°

-73°

-72°

-72°

-71°

-71°

-70°

-70°

-69°

-69°

-68°

-68°

-1° -1°

0° 0°

1° 1°

2° 2°

3° 3°

4° 4°

5° 5°

6° 6°

7° 7°

8° 8°

9° 9°

10° 10°

11° 11°

12° 12°

13° 13°

Fig. 114, HUMA 90-02Fig. 115, HUMA 90-04Fig. 113, TC88-112

Fig. 116, CR88-1100

Fig. 117, CB91-0950

Fig. 118, CA90-1687Fig. 120, MMV Comp. 4

Fig. 121, MMV Comp. 5

Fig. 122, T93-1220

Fig. 134, PW89-1460

Fig. 133, CAQ-8801Fig. 132, OR92-01

Fig. 131, VI92-1200

Fig. 125, CHV-S-91-2

Fig. 123, BP88-03

Fig. 124, BP88-07

Fig. 130, NT92-1090

Fig. 119, TX88-106

Fig. 127, TB-107-87

Fig. 128, EU-02-86

Fig. 112

Fig. 126, RC92-06+T-09

Fig. 129, CP90-1160

EXAMPLE SEISMIC LINES – BASEMAPNote: Disk contains a georeferencedcanvas file and shapefile.

These lines come from the portfoliosof interpreted and uninterpreted seis-mic lines in our report:

“The Colombian Hydrocarbon Habitat”

of which this Atlas forms the first part.

For more information, visit:



Page 79

EXAMPLE SEISMIC LINE – LOWER MAGDALENA BASIN

Fig. 111 Basin: CaribeLine: TC88-112

Fig. 117b Basin: Lower MagdalenaLine: BC91-0950

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