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© 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
-83°
-82°
-81°
-80°
-79°
-78°
-77°
-76°
-75°
-74°
-73°
-72°
-71°
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-83°
-82°
-81°
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-79°
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-70°
-9°
-8°
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-4°
-3°
-2°
-1°0°1°2°3°4°5°6°7°8°9°10°
11°
12°
13°
-9°
-8°
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-3°
-2°
-1°
0°1°2°3°4°5°6°7°8°9°10°
11°
12°
13°
Gua
jira
San
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ama
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ERN
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etre
s
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
Page 2
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
-100°
-100°
-90°
-90°
-80°
-80°
-70°
-70°
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-60°
-50°
-50°
-40°
-40°
-30° -30°
-20° -20°
-10° -10°
0° 0°
10° 10°
20° 20°
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
-100°
-100°
-90°
-90°
-80°
-80°
-70°
-70°
-60°
-60°
-50°
-50°
-40°
-40°
-30° -30°
-20° -20°
-10° -10°
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
Proto-CaribbeanInversion
Zone
FA/NA
Past position ofpresent coastlinein hotspot refer-ence frame
Palinspastic restorationof present coastline
16
-100°
-100°
-90°
-90°
-80°
-80°
-70°
-70°
-60°
-60°
-50°
-50°
-40°
-40°
-30° -30°
-20° -20°
-10° -10°
0° 0°
10° 10°
20° 20°
30° 30°
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
Palinspastic restorationof present coastline
NZ/SA
N. Am.Plate
Past position ofpresent coastlinein hotspot refer-ence frame
NazcaPlate
Proto-CaribbeanInversion
Zone
CaribbeanPlate
17
1000 km
10 Ma
-100°
-100°
-90°
-90°
-80°
-80°
-70°
-70°
-60°
-60°
-50°
-50°
-40°
-40°
-30° -30°
-20° -20°
-10° -10°
0° 0°
10° 10°
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
Palinspastic restorationof present coastline
Past position ofpresent coastlinein hotspot refer-ence frame
N. Am.Plate
AltiplanoS. Am.Plate
CaribbeanPlate
18
-100°
-100°
-90°
-90°
-80°
-80°
-70°
-70°
-60°
-60°
-50°
-50°
-40°
-40°
-30° -30°
-20° -20°
-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
Exploration Framework Atlas Vol. 1 – Colombia © Tectonic Analysis Ltd. 2009
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.
Exploration Framework Atlas Vol. 1 – Colombia © Tectonic Analysis Ltd. 2009
Page 16
-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°
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
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?
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0° 0°
1° 1°
2° 2°
3° 3°
4° 4°
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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.
Exploration Framework Atlas Vol. 1 – Colombia © Tectonic Analysis Ltd. 2009
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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
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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:
http://www.tectonicanalysis.com
Exploration Framework Atlas Vol. 1 – Colombia © Tectonic Analysis Ltd. 2009
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EXAMPLE SEISMIC LINE – LOWER MAGDALENA BASIN
Fig. 111 Basin: CaribeLine: TC88-112
Fig. 117b Basin: Lower MagdalenaLine: BC91-0950
2 of 2
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