palynostratigraphy of the umir formation ...palynostratigraphy of the umir formation, middle...

PALYNOSTRATIGRAPHY OF THE UMIR FORMATION, MIDDLE MAGDALENA VALLEY BASIN (MMVB), COLOMBIA

A ThesisSubmitted to the Graduate Faculty of the

Louisiana State University and Agricultural and Mechanical College

In partial fulfillment of the Requirements for the degree of

Master of Science

in

The Department of Geology and Geophysics

By Carlos E. Santos B.S., Universidad Industrial de Santander, 2005

May, 2012

ii

ACKNOWLEDGEMENTS

I wish to thank Dr. Sophie Warny for giving me the opportunity and the means to complete my

Masters degree and for her very useful advice and continuous guidance.

I also thank the Department of Geology and Geophysics, CENEX Laboratory and the Museum of

Natural Science at Louisiana State University (Baton Rouge, LA) for providing partial funding for

the project.

I want to express my gratitude to the Smithsonian Tropical Research Institute in Panama and the

Colombian Petroleum Institute for their financial and logistical support during my masters.

Thanks go to Dr. Philip Bart and Dr. Alex Webb whose support and service on my advisory

committee were valuable to me.

Special thanks go to my family and friends in Colombia for their continuous and unconditional

support through my masters.

I want to thank specially to E. Alvarez for giving me moral and constant support during the most

difficult moments.

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TABLE OF CONTENTS

ACKNOWLEDGEMENTS......................................................................................................

LIST OF TABLES.....................................................................................................................

LIST OF FIGURES...................................................................................................................

ABSTRACT..............................................................................................................................

1. INTRODUCTION................................................................................................................. 1.1 Campanian-Maastrichtian Palynological Zonations in Colombia and Western Venezuela....................................................................................................... 1.2 Other Maastrichtian Palynological Studies of Colombia and Western Venezuela..................................................................................................................... 2. OBJECTIVE..........................................................................................................................

3. GEOLOGICAL SETTING.................................................................................................... 3.1 Middle Magdalena Valley Basin’s Tectonic and Stratigraphic Framework During the Maastrichtian......................................................................... 3.2 Lithotratigraphy and Depositional Environment of the Umir Formation....................................................................................................................

4. MATERIALS AND METHODS...........................................................................................

5. RESULTS............................................................................................................................... 5.1 Palynology of Core PPI-3........................................................................................... 5.2 Palynology of Core PPM-5......................................................................................... 5.3 Palynology of Core PPM-2......................................................................................... 5.4 Palynology of Core PPM-1.........................................................................................

6. DISCUSSION........................................................................................................................ 6.1 Biostratigraphy............................................................................................................ 6.1.1 Palynological Zone A......................................................................................... 6.1.2 Palynological Zone B......................................................................................... 6.1.3 Palynological Zone C......................................................................................... 6.2 Age assessment and Comparison with Previous Studies............................................ 6.2.1 Pollen and Spores Assemblages......................................................................... 6.2.2 Dinoflagellate Cysts Assemblages...................................................................... 6.3 Paleoenvironmental Interpretation.............................................................................. 6.4 Palynological Record of the Umir Formation and the Global Setting......................... 6.4.1 Dinoflagellate Cyst Assemblages from Umir Formation and

Late Cretaceous Provincialism...........................................................................

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iv

7. CONCLUSIONS...................................................................................................................

REFERENCES.........................................................................................................................

APPENDIX A. QUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN CORE PPI-3 (MIDDLE UMIR FORMATION) EXPRESSED IN ABSOLUTE ABUNDANCES............

APPENDIX B. QUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN CORE PPM-5 (MIDDLE UMIR FORMATION) EXPRESSED IN ABSOLUTE ABUNDANCES............

APPENDIX C. QUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN CORE PPM-2 (MIDDLE - UPPER UMIR FORMATION) EXPRESSED IN ABSOLUTE ABUN-DANCES...................................................................................................................................

APPENDIX D. QUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN CORE PPM-1 (UPPER UMIR FORMATION) EXPRESSED IN ABSOLUTE ABUNDANCES.....

APPENDIX E. RANGE CHART OF SELECTED TAXA IN MIDDLE – UPPER UMIR FORMATION...........................................................................................................................

APPENDIX F. QUANTITATIVE DISTRIBUTION OF PALYNOMORPHS EXPRESSED IN ABSOLUTE ABUNDANCES IN A GENERALIZED COMPOSITE SECTION OF THE MIDDLE – UPPER UMIR FORMATION...............................................................................

APPENDIX G. ILLUSTRATIONS OF SELECTED TAXA IDENTIFIED IN THE UMIR FORMATION...........................................................................................................................

VITA..........................................................................................................................................

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LIST OF TABLES

Table 1 Comparison of four existing Late Cretaceous palynological zonation for Northern South America...........................................................................................................................

Table 2 Comparison between the informal zones proposed for the Late Maastrictian in the Umir Formation and previous Late Cretaceous zonation developed for Northern South America.....................................................................................................................................

Table 3 Significant palynomorph groups used in the paleoenvironmental interpretation.........

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....42

....43

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LIST OF FIGURES

Figure 1 Location of Middle Magdalena Valley Basin (MMVB)..............................................

Figure 2 Generalized stratigraphic column in MMVB..............................................................

Figure 3 Previous Late Cretaceous palynological studies in Central Colombia and Western......................................................................................................................................

Figure 4 Simplified paleogeographic map of Colombia and Western Venezuela during the Maastrichtian.............................................................................................................................

Figure 5 Schematic stratigraphic column of the Umir Formation in San Luis Area, Middle Magdalena Valley Basin............................................................................................................

Figure 6 Location of the cores PPI-3, PPM-5, PPM-2, and PPM-1 in San Luis Area, Los Andes syncline, Central-Eastern MMVB..................................................................................

Figure 7 Composite stratigraphic section of the Middle/Upper Umir Formation in the Los Andes syncline, Central-Eastern MMVB..................................................................................

Figure 8 Relative abundance of significant palynomorph groups in the composite section for Middle – Upper Umir Formation...............................................................................................

Figure 9 Relative abundances of the most abundant palynomorph groups in Core PPI-3.......

Figure 10. Relative abundances of predominant palynomorph groups in Core PPM-5............

Figure 11 Relative abundances of predominant palynomorph groups in Core PPM-2.............

Figure 12 Relative abundances of predominant palynomorph groups in Core PPM-1.............

Figure 13 Zonation and key biostratigraphic events of the Umir formation, San Luis area, Middle Magdalena Valley Basin (MMVB)................................................................................

Figure 14 Paleoenvironmental interpretation of the Umir Formation (Central Eastern MMVB) based on the relative abundance (expressed in percentages) of significant palynomorph groups.........................................................................................................................................

Figure 15 Paleogeographic distribution of Cretaceous conifers and angiosperms based on a fossil wood database...............................................................................................................

Figure 16a Changes in relative abundance (%) of major Cretaceous conifer and angiosperm groups using fossil wood data....................................................................................................

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Figure 16b Changes in relative abundance (%) of gymnosperms and angiosperms based on pollen data from the Late Maastrichtian Umir Formation, Central-Eastern Middle Magdalena Valley Basin...............................................................................................................................

vii

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ABSTRACT

The Late Cretaceous Umir Formation in Middle Magdalena Valley Basin (MMVB)

was recently acknowledged as a new target. However, there is little known about the regional

distribution of the Umir Formation since it is affected by structural complexity and a major

regional unconformity. To improve biosteering of the Umir Formation and reduce exploratory

risks, a detailed biostratigraphic analysis of the Umir Formation in the MMVB is presented. Eighty

samples from four cores drilled in the Central Eastern MMVB were analyzed for palynological

content. These cores represent 976.6 meters of the Middle to Upper Umir Formation.

The sediment yielded a good recovery of pollen, spores and dinoflagellate cysts of

Maastrichtian age, typical of Northern South America. The assemblage is dominated by

species such as Echimonocolpites protofranciscoi, Proteacidites dehaani, Buttinia andreevi,

Spinizonocolpites baculatus, Proxapertites spp., Colombipollis tropicalis, Arecipites regio,

Echitriporites trianguliformis, Echitriporites suescae, Psilatriletes spp., Scabratriletes granularis

and Gabonisporis vigorouxii. Dinoflagellate cyst assemblages include abundances of Andalusiella

and Palaeocystodinium genera and skolochorate cysts dominated by Achomosphaera - Spiniferites

complex. Manumiella seelandica, a dinoflagellate cyst that is a latest Maastrichtian global marker

is recorded for the first time in the MMVB.

Three informal zones (A, B and C) are proposed. Zone A covers the Middle Umir, and

Zones B and C characterize the Upper Umir member. Alternating spikes of peridinoid (Andalusiella

and Palaecosytodinium genera) and skolochorate cysts, and abundances of Echimonocolpites

protofranciscoi and Proxapertites genus characterize layers close and within the Upper Umir

sandstones, showing potential to assist correlations and to evaluate lateral continuity of this new

reservoir.

Based on the palynological assemblages, it is suggested that the Middle Umir Formation

was deposited in a lagoonal environment with coastal swamps and estuarine conditions that evolved

into a semi-restricted bay with river influx for the Upper Umir formation.

viii

Palynological record of the Umir Formation reflects both the drastic replacement of the

gymnosperms by the angiosperms and the Late Cretaceous provincialism of peridinacean dinocysts.

ix

1

1. INTRODUCTION

The Middle Magdalena Valley Basin (MMVB) in Central Colombia is one of the most

productive oil basins in the country. Thus far, oil exploration has been mainly focused on

Eocene - Oligocene clastic reservoirs (Figure 1). In the MMVB petroleum system, the Upper

Cretaceous formations have been

traditionally considered to form the

seal of the stratigraphic traps with

Lower Cretaceous reservoirs (Prince

et al., 2011). The Upper Cretaceous

formations also serve as seals in west-

verging thrusts that overlap Cenozoic

reservoirs. In Paleogene and Neogene

plays (areas in which hydrocarbon

accumulations or prospects of a given

type occur), the Upper Cretaceous

formations are considered the economic

basement (Prince et al., 2011); i.e. the

rock layers below which economic

hydrocarbon reservoirs are not expected

to be found.

In this mature basin, ongoing

oil exploration focuses on complex

structural areas such as the Western

foothills of the Eastern Cordillera

(Villamil, 2003) and Cretaceous

sequences (Córdoba et al., 2000; Prince

et al., 2011). The Late Cretaceous Umir

id le M dM gda enaa l

V lley Basi a n(MMVB)

Bogota D.C

Lower Magdalena

Valley

LlanosBasin

Bucaramanga

-72°30´ -71°40´-73°20´-74°10´-75° W

9°1

0´

N8

°20

´7

°30

´6

°10

´5

°50

´5

°4

°10

´

Venezuela

0 100 Km

N

San Luis Oil Field

Santa Lucíaoil field

CaribbeanSea

SouthAmerica

PacificOcean

Venezuela

EcuadorBrazil

Peru

PacificOcean

CaribbeanSea

Panama

Los Andes Syncline(San Luis Area)

Figure 1. A) Location of Middle Magdalena Valley Basin (MMVB). Red areas correspond to exploratory blocks where the Umir Formation is targeted. In Santa Lucía and San Luis fields, the Umir Upper sandstones are oil producers.

2

formation has become a new target since it has produced oil in Santa Lucia and San Luis oil fields

(Ortiz and Flórez, 1997, see Figure 2).

Interest in this target has also peaked since Prince et al. (2011) defined a new Aptian-

Maastrichtian petroleum system containing the Umir Upper sandstones as a reservoir. Despite the

recent increased interest of oil companies in this formation, the main problem for exploration lies

within the high structural complexity of the unexplored western foothills of the Eastern Cordillera

and the presence of the Middle Magdalena Valley Unconformity. As a result, there is little known

Figure 2. Generalized stratigraphic column in MMVB (from Ecopetrol, 2009). See Figure 1 for location.

Oil FieldsMiocene

Eocene

Paleocene

Maast.

Camp-Sant.

Coniacian

Turonian

Cenomanian

Albian

Aptian

Jurassic

Jordan

Giron

Tambor

Los Santos

Rosablanca

Cumbre

Salto

Paja

Tablazo

Simití

La Luna

Umir

Lisama

La Paz

Esmeraldas

Mugrosa

Colorado

Real

Mesa

Fm.Age

Valang.

Barremian

Berrias.

Oligocene

Pliocene -Pleistocene

Llanito, Infantas

Infantas, Lisama, PerolesNutria, TesoroProvincia, Libre

Provincia, Opón,Cantagallo

Provincia, Bonanza

Santa Lucía, San Luis

Buturama

Catalina

Proved Reservoir

Potential Reservoir

Source rock

3

on this new reservoir and its regional distribution, so exploratory risks are high. This is despite

the fact that a large number of palynological studies have been published for the Late Cretaceous

in Colombia (e.g. Germeraard et al., 1968; Sole de Porta, 1972; Muller et al., 1987; Sarmiento,

1992; Yepes, 2001; Pocknall, 2001; Jaramillo and Rueda, 2004). But in reality, just a few projects

have focused on the Middle Magdalena Valley Basin (e.g. Van der Hammen, 1954; Van der

Hammen, 1957; Germeraard et al., 1968; Sole de Porta, 1971). The scarcity of publications on the

palynostratigraphy of the Umir formation is most likely due to the earlier lack of interest in the

Umir Formation from the oil industry, as these companies (e.g., Ecopetrol, SHELL, BP) lead and

funded most of the geological research that has been done in the basin.

Hence, this research project specifically aims to build the biostratigraphic framework for

the Late Cretaceous Umir Formation in the MMVB to enhance geological distribution models

and reduce exploratory risks. Palynology is the best micropaleontological proxy for the Umir

Formation since depositional conditions allowed for preservation of abundant terrestrial (pollen

and spores) and marine (dinoflagellate cysts and acritarchs) palynomorphs. Additionally, as

discussed above, palynology has been a successful tool (Figure 3) in solving problems associated

with oil exploration in Colombian basins for the past 40 years (Germeraard et al., 1968; Sole de

Porta, 1972; Mullet et al., 1987; Jaramillo and Rueda, 2004; Jaramillo et al., 2006; Torres et al.,

2008; Contreras et al. 2010; Jaramillo et al. 2011).

The major biostratigraphic events defined via this study will be used to develop regional

correlations and will serve as a key tool for on-site, real-time biostratigraphic control of future

MMVB exploratory wells.

1.1 Campanian-Maastrichtian Palynological Zonations in Colombia and Western Venezuela

Maastrichtian palynological studies in Colombia and Western Venezuela have led to the

development of four zonal schemes defined by Van der Hammen (1954; 1957), Germeraard et al.

(1968), Muller et al. (1987) and Sarmiento (1992). Figure 3 provides the location of each study

sections while Table 1 summarizes the four zonations.

4

Van der Hammen (1954; 1957) studied the Guaduas Formation (Sutatauza area, Eastern

Cordillera) and the Umir Formation (Middle Magdalena Valley basin) in Colombia and proposed

3 zones and 8 subzones for the Maastrichtian (Table 1, Figure 3). The zones were defined

considering changes in the abundance of three main groups: the Psilatriletes group, including all the

Psilatriletes spores; the Monocolpites medius group, composed mostly of Monocolpites minutus,

Monocolpites huertasii and Monocolpites medius; and the angiosperms group, that include four

genera; Tricolpites, Triporites, Tricolporites and Stephanocolpites. According to Van der Hammen

(1954), the zonal changes reflect climatic or evolutionary events. For instance, the increase of

Figure 3. Previous Late Cretaceous palynological studies in Central Colombia and Western Venezuela. Note the absence of studies in Middle Magdalena Valley Basin.

-74.0-76.0 W -72.0

8°

6°

4°

2° N

Upper Magdalena

Valley

Colombia

MiddleMagdalena

ValleyBasin

Venezuela

Bogota D.C

Bucaramanga

Sole de Porta (1971; 1972)

De la Parra (2009)

Germeraard et al. (1968)Muller et al. (1987)

0 100 Km

N

Van der Hammen (1954; 1957)

Yepes (2001)

Sarmiento (1992)

Pocknall et al. (2001)

CaribbeanSea

SouthAmerica

PacificOcean

Venezuela

Ecuador

Brazil

Peru

PacificOcean

CaribbeanSea

Panama

5

arboreal pollen up section is interpreted as being related to the radiation of angiosperms (Van der

Hammen, 1954) in late Cretaceous. The zonation was calibrated using Maastrichtian foraminifera

and ammonites from both the lowest zone (Maastrichtian A1 zone, Middle Magdalena Basin)

and the uppermost zone (Maastrichtian C zone, Catatumbo basin) (Van der Hammen, 1957).

Campanian associations were not recognized.

This pioneer work is no longer considered valid since the palynological systematic

nomenclature has changed considerably in the last fifty years, and morphotypes described by Van

der Hammen (1954; 1957) have been revised and associated to other genera. For instance, the

species Monocolpites humbertoides initially described as a monocolpate pollen was amended

as a zonosulcate grain belonging to Proxapertites genus (Sarmiento, 1992). Additionally, with

the increase of palynological knowledge, the stratigraphic range of some taxa has changed, and

palynomorphs previously considered exclusively Maastrichtian have been found in younger

sediments.

AGE

TROPICAL ZONE NORTHERN SOUTH AMERICA

COLOMBIA

MIDDLE MAGDALENA

VALLEY BASIN

PALEOCENE

LA

TE

CR

ET

AC

EO

US

MA

AS

TR

ICH

TIA

N

DANIAN

CA

MP

AN

IAN

Caribbeanzones

Atlantic zones

Pantropicalzones

Zone 11Auriculiidites reticularis

Zone 14Spinizonocolpites baculatus

Zone 12Crassitricolporites subprolatus

MaastrichtianA

MaastrichtianB

MaastrichtianC

PaleoceneA

PaleoceneB

Zone 15Gemmastephanocolpites gemmatus

Zone 13Proteacidites dehaani

Zone 16Foveotricolpites perforatus

Proteacidites dehaani

Retidiporites magdalenensis

Proxapertites operculatus

Foveotriletes margaritae

Ctenolophoniditeslisamae

Foveotricolporitesperforatus

EASTERN CORDILLERA

Zone IIa Zonotricolpites variabilis

Zone IIb Syncolporites lisamae

Zone 1Buttinia andreevi

Sarmiento (1992)Van der Hammen

(1954; 1957)

Muller, de Giacomo and Van Erve (1987)

Germeraard, Hopping and Muller (1968)

Table 1. Comparison of four existing Late Cretaceous palynological zonations for Northern South America (modified from Pocknall et al., 2001).

5 6

Germeraard et al. (1968) analyzed data from Africa, Northern South America and Borneo

and proposed the first palynological zonation for Tertiary sediments in tropical areas. Although this

classic zonal scheme was focused mainly on the Cenozoic, Germeraard et al. (1968) defined the

zone Proteacidites dehaani for the Maastrichtian. The zone was characterized by the co-occurrence

of Proteacidites dehaani and Jugoperiporites gutjahri plus high abundances of Foveotriletes

margaritae. The base of this zone was not established, but the top, marked by the last occurrence of

Proteacidites dehaani, was clearly identified inside the Orocue Formation in Western Venezuela.

In Colombia, this zone was recognized in the Colon Mito-Juan Formations (Catatumbo Basin,

Northern Colombia) and in the Umir formation (Middle Magdalena Valley Basin). The Zone

Proteacidites dehaani was calibrated using foraminifera assemblages and ammonites recovered

from its lower section (Germeraard et al., 1968).

Muller et al. (1987) analyzed palynological data from Colombia, Venezuela, Trinidad,

Guyana, Surinam and Brazil and proposed a zonation for the Late Cretaceous - Cenozoic in

Northern South America. The chart contains six superzones for the Cretaceous, including

the super zone VI for the Campanian - Maastrichtian interval (Table 1). The zonation was

calibrated using the same criteria employed by Germeraard et al. (1968). Super zone VI was

divided by Muller et al. (1987) into three zones: the Zone 11 Auriculidites reticularis, the Zone

12 Crassitricolporites subprolatus, and the Zone 13 Proteacidites dehaani (Table 1). Zone 11

(Auriculidites reticularis), covering the Campanian–lowermost Maastrichtian, was characterized

as a taxon-range zone. Its base was defined by the last occurrence of Droseridites senonicus plus

the first occurrences of Auriculiidites reticularis and Buttinia andreevi, and its top by the last

occurrence of Auriculiidites reticularis. The zone was based on data from a well located in the

Faja Petrolifera del Orinoco in Venezuela and has an equivalent in Brazil (Muller et al., 1987).

Zone 12 (Crassitricolporites subprolatus) covers part of the Maastrichtian (Table 1) and is based

on data published by Regali et al. (1974) for the Campos Basin, Brazil. Its base corresponds to

the last occurrence of Auriculiidites reticularis and its top to the first occurrence of Proteacidites

dehaani. Biostratigraphic events occurring within this zone include the first occurrences of

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Crassitricolporites subprolatus, Aquillapollenites, Scollardia, Retidiporites magdalenensis,

Proxapertites group and Ilexpollenites; and last occurrences of Crassitricolporites subprolatus,

Crassitricolporites brasiliensis, Ariadnaesporites complex and Zlivisporis blanensis in the top of

the zone. Zone 13 (Proteacidites dehaani) was defined by the first occurrences of Proteacidites

dehaani at its base and Spinizonocolpites baculatus at its top. Biostratigraphic events occurring

in this zone are the first appearance data of Foveotriletes margaritae, Stephanocolpites costatus,

Proxapertites operculatus group, Spinizonocolpites group, Ulmoideipites genus, Spinizonocolpites

intrarugulatus sp. nov and Gemmamonocolpites macrogemmatus; and last occurrences of Buttinia

andreevi, Proteacidites dehaani, Crassitricolporites brasilliensis, Aquilapollenites and Scollardia.

This zone corresponds to the late Maastrichtian and its top marks the important Cretaceous-Tertiary

boundary. The reference section for Zone 13 is located in Western Venezuela inside the Guasare

formation, and it was recognized in Colombia, in the Catatumbo basin inside the Colón and Mito-

Juan formations (Muller et al., 1987).

Muller´s zonation provided a good palynostratigraphic framework for Northern South

America. Nevertheless, its use for the Late Cretaceous of the Middle Magdalena Valley Basin

is restricted as the zonation was mostly based on data from Brazil and Venezuela. Only one of

the three zones proposed for the Campanian – Maastrichtian interval, the Zone 13 Proteacidites

dehaani includes data from Colombia and was recognized in the Catatumbo basin. Furthermore,

some of the taxa used in the zonation have not been recorded in Middle Magdalena Valley Basin,

and the stratigraphic range of others has changed or is longer in this basin most likely as a result

of environmental differences.

A palynogical zonation based exclusively on data from Colombia was published by

Sarmiento (1992). He analyzed a stratigraphic section of the Guaduas Formation in the Eastern

Cordillera and proposed a zonation for the Maastrichtian - Paleocene interval for Central Colombia

(Table 1, Figure 3). In his research, Sarmiento (1992) identified 79 palynomorphs including 9 new

genus, 33 new species and 6 new combinations. This work constitute the basis of the systematic

nomenclature used in subsequent palynological studies on the Maastrichtian - Paleocene of

8

7 8

Colombia. His zonation includes two zones: Zone I (Buttinia andreevi) for the Maastrichtian;

and Zone II (Foveotriletes margaritae) for the Paleocene (Table 1). Zone I (Buttinia andreevi)

was characterized by high abundance of Psilatriletes guaduensis, Psilamonocolpites medius and

Psilatricolporites rubini (Sarmiento, 1992; 1994). Taxa restricted to this zone are Echimonocolpites

echiverrucatus, Spinizonocolpites echinatus, Retimonocolpites claris, Crusafontites grandiosus,

Clavatriletes mutisii, Inaperturopollenites cursi, Psilamonocolpites ciscudae and Retitricolpites

Belskii. Occurrences of Annutriporites iversenii, Proxapertites humbertoides, Retidiporites

magdalenensis, Buttinia andreevi, Bacumorphomonocolpites tausae, Ephedripites multicostatus,

Stephanocolpites guaduensis, Echimonocolpites protofranciscoi and Retitricolpites josephinae are

also frequent. At the top of the zone, Buttinia andreevi disappeared but is recorded again at the

top of Zone IIA (Sarmiento, 1992). Zone I (Buttinia andreevi) is correlated to the Maastrichtian

zone A of Van der Hammen, (1954; 1957), the Proteacidites dehaani zone of Germeraard et al.,

(1968) and the Zone 13 of Muller et al. (1987) (Table 1). Zone II (Foveotriletes margaritae)

includes two subzones: Subzone IIA Zonotricolpites variabilis and Subzone IIb Syncolporites

lisamae (Table 1). Sarmiento (1992) suggested that the boundary between Zones I and II

corresponds to the Cretaceous – Tertiary boundary, but an abrupt palynological change expected

to evidence the K/T boundary was not recognized. This said, the first appearances of 38 species

occur immediately below or within Subzone IIA. A few first appearances were found below the

boundary (i.e. Proxapertites psilatus, Gemmamonocolpites dispersus, Syndemicolpites typicus,

Foveotriletes margaritae, Longapertites vaneendenburgi and Racemonocolpites racematus); others

at the boundary (i.e. Longapertites perforatus, Psilabrevitricolporites annulatus, Mauritiidites

franciscoi, Zonotricolpites variabilis); and some above the boundary (i.e. Echimonocolpites coni,

Retitricolporites exinamplius, Proxapertites verrucatus and Proxapertites operculatus). The base

of the Subzone IIB (Syncolporites lisamae) is marked by the last occurrences of Duplotriporites

ariani, Bacumorphomonocolpites tausae, Ephedripites multicostatus, Araucariacites australis and

Zlivisporis blanensis; and the first occurrences of Syncolporites lisamae, Spinizonocolpites tausae

and Psilatriletes martinensis. Occurrences of Foveotriletes margaritae, Divissisporties enormis,

9

Echitriporites trianguliformis and Gemmamonocolpites dispersus were also recorded inside

Subzone IIB. Sarmiento (1992) correlated zone II (Foveotriletes margaritae) to the Maastrichtian

Zones B and C of Van der Hammen (1954; 1957), and to the Danian zones Foveotriletes margaritae

of Germeraard et al. (1968) and the Zone 14 Spinizonocolpites baculatus of Muller et al. (1987)

(Table 1).

Although the systematic palynology published by Sarmiento (1992) is a reference for any

Maastrichtian – Paleocene palynological studies in Colombia, the pollen zones and ages published

are controversial. Zone I Buttinia andreevi was correlated to Zone Proteacidites dehaani of

Germeraard et al. (1968) and Muller et al. (1987) despite the fact that Proteacidites dehaani, the key

marker defining this zone, was not recorded in the Guaduas section. Sarmiento (1992) clarified that

the correlation was done considering the stratigraphic position and not pollen assemblages. Other

inconsistencies in Sarmiento´s work relates to zone II Foveotriletes margaritae, dated as Danian

and correlated to zones Foveotriletes margaritae of Germeraard et al. (1968) and Muller et al.

(1987). Muller et al. (1987) defined the base of the zone by the first occurrence of Spinizonocolpites

baculatus, and the top by the first occurrence of Gemmastephanocolpites gemmatus. In the Guaduas

section, Spinizonocolpites baculatus has a wider stratigraphic range and Gemmastephanocolpites

gemmatus was not recovered. The acme (high abundance) of Proxapertites operculatus, a

diagnostic event recognized regionally in the lower Paleocene of Colombia was not mentioned

either by Sarmiento (1992). Rather he identified occurrences of Araucariacites australis, Tetradites

umirensis, Colombipollis tropicalis, Ulmoideipites krempii, Periretisyncolpites giganteus,

Buttinia andreevi, Bacumorphomonocolpites tausae and Duplotriporites ariani both in the zone I

(Maastrichtian) and zone II (Danian). In fact, the top of the subzone IIA (still Danian) was defined

by the last occurrence of Buttinia andreevi, Bacumorphomonocolpites tausae, Duplotriporites

ariani and Araucariacites australis. Later studies showed that most of these taxa occur in the Late

Maastrichtian, and became extinct in the K/T boundary (De la Parra, 2009).

10

9 10

1.2 Other Maastrichtian Palynological Studies of Colombia and Western Venezuela.

Other biostratigraphic studies of the Maastrichtian of Colombia and Venezuela described

palynological assemblages and new morphotypes (Sole de Porta, 1971; 1972) and provided a

detailed analysis of the K/T boundary palynological changes in the region (Yepes, 2001; Pocknall,

2001; De la Parra 2009) (Figure 3).

Sole de Porta (1971) described palynological assemblages from the Maastrichtian - Paleocene

Guaduas Formation (Eastern Cordillera) identifying four new genus (Baculamonocolpites,

Bacumorphomonocolpites, Crusafontites, and Foveomorphomonocolpites), two new species

(Bacumorphomonocolpites tausae and Crusafontites grandiosus) and new sub-species for

Leiotriletes guaduensis, Baculamonocolpites espinosus and Foveomorphomonocolpites

humbertoides.

Sole de Porta (1972) analyzed the Cimarrona Formation (Zaragoza and Primavera members)

in the Southern Middle Magdalena Valley Basin. Two palynological assemblages including

occurrences of Proteacidites dehaani, Buttinia andreevi, Foveotriletes margaritae, Cyatheacidites

vanderhammeni, Leiotriletes guaduensis, Muerrigerisporis americanus, Schizeaoisporites

cicatricos, Baculamonocolpites minimus, Bacumorphomonocolpites tausae, Annutriporites

iversenii, Annutriporites annulatus, Echimonocolpites minutispinosus, Foveomorphomonocolpites

humbertoides, Retidiporites magdalenensis, Magnatriporites umirensis, Plicapollis bellus

and Monoporisporites grandis, among others, were identified. The assemblages, dated both as

Maastrichtian, were calibrated using micropaleontological analysis conducted by De Porta (1966),

and were correlated to the Proteacidites dehaani zone of Germeraard et al. (1968).

Yepes (2001) analyzed the Río Molino section in Northern Colombia (in the Cesar

Rancheria Basin) and the Río Loro section in Western Venezuela, where the Colon and Mito-

Juan formations are exposed (Figure 1). Using dinoflagellates cyst assemblages, he identified

biostratigraphic events that provide a mean to differentiate Upper Campanian from Lower and

Upper Maastrichtian, and provide the basis to place the K/T boundary. To establish the Upper

Campanian - Lower Maastrichtian boundary, Yepes (2001) used the highest occurrences of

11

Xenascus ceratioides, Odontochitina operculata, Trichodinium castanae, Hystrichodinium sp.

and Palaeohystrichophora infusorioides; and the lowest occurrences of Areoligera senonensis,

Cerodinium diebelii, Trithyrodinium evittii, Yolkinigymnium lanceolatum, Phelodinium tricuspe,

Cordospaheridium fibrosum, Andalusiella spp., Seleganium sp. Palaeocystodinium spp. and

Palaeocystodinium australinum. The upper Maastrichtian was characterized using the occurrences

of Dispharogena carposphaeropsis, Glaphyrocysta perforate, Manumiella seelandica and

Thalassiphora patula. Yepes (2001) recognized the K/T boundary using the lowest occurrences of

Damassidinium californicum and Senoniasphaera inornata that are restricted to the Danian (Early

Paleocene). Even though, Maastrichtian biostratigraphic studies based on dinoflagellates cysts are

scarce in Northern South America, Yepes (2001) found key dinoflagellate events that correlate to

known biomarkers of global significance. The events he described were calibrated with calcareous

nannofossils and planktonik foraminifera events reported by Martinez (1989) and Martinez and

Hernández (1992) for the Río Molino section.

Poknall et al. (2001), using graphic correlation in the Rio Loro Section (Western Venezuela),

calibrated the terrestrial palynological record of the Maastrichtian – Paleocene interval with

dinoflagellate cysts assemblages from the Amoco’s corporate global database. As a result, these

authors differentiated assemblages for the Lower and Upper Maastrichtian and for the Danian.

The Lower Maastrichtian was characterized by abundances of Cyathidites australis and Mauritia

crassibaculatus; minor frequencies of Spinizonocolpites baculatus, Echitriporites trianguliformis,

Proxapertites spp., Arecipites spp., and Foveotriletes margaritae; and the first appearances of

Colombipollis tropicalis and Kleithosphaeridium truncatum. The dinoflagellate assemblage was

dominated by occurrences of Palaeocystodinium golzowense and Andalusiella spp. Pocknall et al.

(2001) recognized abundances of Palaeocystodinium golzowense, Glaphyrocysta perforatum and

Andalusiella polymorpha in Middle Maastrichtian assemblages. Low frequencies of Cyathidites

australis, Foveotriletes margaritae and Proxapertites spp., and the last occurrence of Dinogymnium

pustulicostatum were also recorded. The latest Maastrichtian was defined by occurrences of

Glaphirocysta perforatum and Dinogymnium pustule, and abundance of Arecipites spp, Cyathidites

12

11 12

australis, Foveotriletes margaritae, Mauritia crassibaculatus, Proteacidites spp., Proxapertites

spp., Spinizonocolpites baculatus and Spinizonocolpites echinatus. Finally, occurrences of

Damassidinium californicum, Fibrocysta bipolaris, Kenleyia lophophora, Turbiosphera filose,

Carpatella cornuta and Caslidinium fragile defined the Early Danian.

As Sarmiento (1992), Pocknall et al. (2001) recorded occurrences of Proteacidites

dehaani, Crusafontites grandiosus, Periretisyncolpites giganteus and Araucariacites australis in

the Paleocene. Buttinia andreevi, one of the key Maastrichtian taxa, was not recorded.

De la Parra (2009) analyzed the K/T boundary in a stratigraphic section in Cesar-Rancheria

basin (Northern Colombia) by using several statistical techniques to estimate extinction percentages

and changes in diversity related to the boundary (Figure 1). He calculated an extinction percentage

of 48-70% and showed that the high diversity Cretaceous palynoflora was replaced by a low

diversity Paleocene assemblage. Some of the species that became extinct at the boundary include

Echimonocolpites protofranciscoi, Buttinia andreevi and Protecidites dehaani, restricting their

range to the Late Cretaceous (De la Parra, 2009).

In summary, several studies and zonal schemes have proposed biostratigraphic events

for the late Cretaceous in Colombia and Western Venezuela (Van der Hammen, 1954; Van der

Hammen, 1957; Germeraard et al., 1968; Sole de Porta, 1971; Sole de Porta, 1972; Muller et al.,

1987; Sarmiento, 1992; Yepes, 2001; Pocknall, 2001; De la Parra, 2009) however, only a few

have been conducted on the Umir Formation in Middle Magdalena Valley Basin (Germeraard

et al., 1968; Van der Hammen, 1954; Van der Hammen, 1957; Sole de Porta, 1972). Applying

these zonations in Middle Magdalena Valley Basin is constrained by inconsistencies in systematic

nomenclature, differences in the stratigraphic range of some taxa in the basin, and the absence

of some of the events due to facies changes. Hence, analyze the palynological content of the

Umir Formation in order to develop a palynostratigraphic framework for the Late Cretaceous

in the Middle Magdalena Valley Basin is long overdue and is the specific focus on this thesis.

The zonation developed will provide a detailed biostratigraphic framework that will be correlated

throughout the basin and contextualized using the regional palynological frame.

13

2. OBJECTIVE

The aim of this project is to conduct a detailed palynological analysis of one composite

section encompassing the Umir formation in Middle Magdalena Valley Basin to develop a

biostratigraphic framework for the Late Cretaceous Umir Formation. Major biostratigraphic

events will be used to develop regional correlations, and serve as a key tool for on-site, real-time

biostratigraphic control of exploratory wells.

14

14

3. GEOLOGICAL SETTING

The Middle Magdalena Valley Basin (MMVB) is an intermontane basin located between

the Central and Eastern Cordilleras in Central Colombia (Figure 4). From the Triassic to the Middle

Miocene, the MMVB used to be part of a larger regional basin made off the Eastern Cordillera and

the Llanos basin (Cooper et al., 1995; Villamil, 1999; Gómez at al., 2005). The development of the

Central Cordillera (to the west), the Eastern Cordillera (to the East) and the tectonic evolution of

the Northwestern Margin of South America had a major impact on the MMVB formation (Cooper

et al. 1995; Gomez et al., 2003; Rolón, 2004; Gomez et al., 2005). The tectonic development of this

basin can be summarized in four main events: 1) Triassic – Aptian rifting; 2) Early Cretaceous –

Campanian thermal subsidence; 3) Late Cretaceous - Early Eocene uplift of the Central Cordillera;

and 4) Middle Miocene – Recent uplift of the Eastern Cordillera (Cooper et al. 1995; Villamil,

1999; Gómez et al. 2005; Rolón 2004).

The Triassic to Earliest Cretaceous rifting phase was related to the separation of North and

South America (Cooper et al., 1995). The synrift megasequence is represented by 3000 to 5000

meters of Jurassic red beds and volcaniclastic strata in the Eastern Cordillera and MMVB (Gómez

et al., 2003). By Early Cretaceous, the initial Jurassic continental environments were replaced by

sequences indicative of paralic (deposits laid down on the landward side of a coast) and shallow

marine conditions (Cooper et al., 1995).

During the Early Cretaceous to Campanian, the MMVB underwent thermal subsidence

associated with a back-arc setting. As a consequence, a marine transgression flooded the Colombian

Cretaceous basin depositing a sequence of shales, mudstones and chert beds (Cooper at al., 1995).

The rise of sea level coupled with anoxic conditions and upwelling led to the deposition of a series

of organic-rich mudstones, cherts and phosphates that constitute the most prolific source rock in

Northern South America (Cooper et al. 1995; Gómez et al. 2005).

Later in the Early Maastrichtian, the diachronous accretion of the Western Cordillera

caused the initial uplifting of the Central Cordillera and the beginning of the inversion of Triassic

- Jurassic extensional faults (Gomez et al. 2005). Shortening continued until the Early Eocene

15

and produced an abrupt change in the depositional environments in the Middle Magdalena Valley

Basin, the Eastern Cordillera, and the Llanos Basin (Cooper et al., 1995; Gómez et al., 2003;

Gómez et al., 2005). Conditions were predominantly marine during most of the Cretaceous, then

became transitional for the Latest Cretaceous – Paleocene and fluvial in the Early Eocene. These

coarsening upward sequences consist of shallow marine, coastal plain, estuarine, coal-rich alluvial

plain and alluvial fan deposits (Cooper et al., 1995; Gómez et al., 2003). Since the initial uplift

of the Central Cordillera during the Late Cretaceous, the deformation associated with the uplift

migrated eastward until the Early Eocene. The propagation of the deformation combined with the

ending of the Central Cordillera uplift in the Early Eocene resulted in a key stratigraphic feature:

the Middle Magdalena Valley unconformity (MMVU) (Gómez et al., 2003; Gomez et al., 2005).

The MMVU separates Mesozoic and Paleocene units from the Middle Eocene and

Neogene formations (Gómez et al., 2003; Gomez et al., 2005). This regional unconformity dips

eastward to the Eastern Cordillera and is continuous to the west in the Central Cordillera. The

stratigraphic hiatus associated with the MMVU decreases toward the east. Preserved thicknesses

of both the Mesozoic/Paleocene sequence and the onlapping Middle Eocene/ Neogene sequence

increase eastward, to the western foothills of the Eastern Cordillera (Gómez et al., 2003; Gomez

et al., 2005) (Figure 4). The thickness of these sequences decreases northward to the Cáchira Arch

(Gómez et al., 2003; Gomez et al., 2005), while the time gap associated with the unconformity

decreases toward the east. This trend is recorded regionally throughout the MMVB (Figure 4)

(Gómez et al., 2003; Gomez et al., 2005).

The major deformation of the Eastern Cordillera and Llanos Foothills started in the Middle

Miocene and continued until the Pliocene. It resulted from the collision of the Panamá - Baudó

arc with the northwestern margin of South America (Dengo and Covey, 1993; Cooper et al., 1995;

Gómez et al., 2003; Gómez et al., 2005). This intense tectonic pulse reactivated and finalized the

tectonic inversion of the Jurassic extensional faults and created new compressional structures,

including thrust fans and triangle zones in the Llanos foothills (Cooper et al., 1995; Rolón, 2004).

As a consequence the Eastern Cordillera was uplifted and eroded (Cooper et al., 1995; Gómez et

16

15 16

al., 2003; Gómez et al., 2005) and the Llanos Basin and Middle Magdalena Valley Basin became

isolated (Cooper et al., 1995). At this stage, the MMVB acquired its current configuration.

Figure 4 Simplified paleogeographic map of Colombia and Western Venezuela during the Maastrichtian (Adopted and modified from Villamil, 1999). The dot-lined arrow indicates the location of the depocenter in the basin during the Campanian. Notice how the depocenter migrated from a western location (in Eastern Central Cordillera) to a central location in the Maastrichtian (Villamil, 1999).

-74.0-76.0-78.0 -72.0-80.0 W

12°

8°

6°

10°

4°

2° N

CaribbeanSea

SouthAmerica

PacificOcean

Ac

r

nes

tral

Cen

tral

Co

dill

era

Cen

tra

axi

s of

de

ositi

on

l

p

Bogota

Venezuela

UmirAlluvial fans

Shelf shales

Shallow water marine

Coastal and fluvial

Campanian center of deposition

MMVB

CaribbeanSea

N

Ecuador

Colombia

PacificOcean

0 100 Km

N

17

3.1. Tectonic and Stratigraphic Framework for the Maastrichtian in Middle Magdalena

Valley Basin

As mentioned above, the initial uplift of the Central Cordillera during the Early Maastrichtian

by accretion of the Western Cordillera produced a dramatic change in the depositional environments

of the Middle Magdalena Valley Basin, Eastern cordillera and Llanos Basin (Cooper et al. 1995;

Villamil, 1999; Gómez et al., 2003; Gómez et al., 2005). Predominantly marine conditions were

replaced by coastal plain and deltaic environments. Campanian-Maastrichtian rocks in the MMVB

recorded the northward withdrawal of the sea in North Western South America. This regression

continued into the late Maastrichtian and Early Paleocene (Villamil, 1999; Gómez et al. 2003). The

major mechanisms controlling the sedimentation in this large basin during these periods were the

eastward migration of the center of deposition and the decrease of accommodation space (Villamil,

1999).

During the Campanian, the depocenter axis of the basin was located along the Eastern

foothills of the Central Cordillera and the westernmost area of the MMVB. Epicontinental seas

covered eastern Colombia and western Venezuela and distal facies were deposited in the north

and west (Villamil, 1999). After the initial Early Maastrichtian uplift of the Central Cordillera, the

position of the depocenter switched to a new location along the western foothills of the Eastern

Cordillera (Villamil, 1999). Hence, a new Maastrichtian marine seaway with a NE-SW orientation

was created. Facies deposited in Middle Magdalena Valley basin were very close to the depocenter

and consisted mostly of shales, mudstones and claystones forming the Umir Formation (Villamil,

1999). The Buscavidas shale in Southern MMVB and Colon Mito-Juan formations in the Catatumbo

Basin represent similar facies and are correlated with the Umir. In eastern and westernmost areas,

discontinuous coarse clastic sediments were deposited, including the Cimarrona formation in

southeastern MMVB (Villamil, 1999).

3.2. Lithotratigraphy and Depositional Environment of the Umir Formation

The Umir formation was originally described by Morales (1958) as a series of dark, bluish-

18

17 18

gray and black thin bedded shales for the lower section; and dark gray thin-bedded shales with

several coal beds and intercalations of fine-grained sandstones and siltstones in the upper section.

In the type locality, its thickness corresponds to approximately 1000 m. The contact of the Umir

formation with the underlying La Luna formation is slightly unconformable; and it is conformable

with the overlying Lisamae Formation (Morales, 1958).

A detailed study by Ecocarbón (1996) conducted in the San Luis area, in the Los Andes

Syncline (central MMVB), differentiated three intra-Umir members (Figure 5). The lower member

is characterized by a series of blue-grayish to black mudstones with thin bedding, alternated with

nodular ferruginous siltstones and carbonate with micaceous laminations. Coal beds were not

recognized in this member. The boundary

with the middle member was defined on the

first occurrence of coal beds. This overlying

middle member consists of black to gray shales

alternating with ferruginous siltstones and coal

beds with thicknesses ranging from a few

centimeters to 3 meters. The limit between the

middle and upper members corresponds to a

12 meter-thick sandstone. The Upper member

is composed of light gray to black carbonate

mudstones and black to gray mudstones

alternating with siltstones and shales and

include upt to 31 coal beds in the lower part and

coal beds up to 0.6 meters in thickness in the

middle part. Fine to middle grained sandstones

were also identified. The total thickness of the

Umir Formation in this region is estimated to

be approximately 1400 meters.

Figure 5 Schematic stratigraphic column of the Umir Formation in San Luis Area, Middle Magdalena Valley Basin.

Upper

Um

irM

iddle

Um

irLow

er

Um

ir

Limestone

Mudstone, Shale

Siltstone

Coal

Sandstone

19

Ortiz and Flórez (1997) conducted a sequence stratigraphic analysis of the Umir formation

using cores collected by Ecocarbón (1996). Two distinct facies were defined: the lake-fill facies

consisting of shales, coal beds, and laminated mudstones and siltstones; and the channel - crevasse

splay facies made of intraformational conglomerates, crossed-stratified sandstones, laminated

sandstones and siltstones. Four low frequency cycles were identified. The lake-fill facies

predominates in the basal three cycles; and in the uppermost cycle, the channel - crevasse splay

facies is dominant. The vertical distribution of the facies marks a decrease of accumulation space

within the Umir (Ortiz and Flórez, 1997). Based on this model, Ortiz and Flórez (1997) interpreted

the depositional environment for the Umir Formation either as a bay with paralic conditions or a

semi-restricted lagoonal area, with channel influence in the area close to coastline.

In its original description, to the Umir formation was assigned a Campanian –

Maastrichtian age (Morales, 1958; Julivert, 1968). Petters (1955), using foraminiferal assemblages

from Western Venezuela recognized, from base to top, the zones Siphogenerinoides cretacea,

Siphogenerinoides bramlettei and Ammobaculites colombianus. The report of the Campanian

ammonite Stantonoceras associated with the Siphogenerinoides cretacea zone, in the Southern

Upper Middle Magdalena Valley, supported the Campanian age for the base of the Umir (Morales,

1958). Maastrichtian ammonites within the Siphogenerinoides bramlettei and Ammobaculites

colombianus zones confirmed the Maastrichtian age for the rest of the formation (Petters, 1955).

Nevertheless, Tchegliakova (1995; 1996) revaluated the Campanian age assigned to the

Lower Umir. Tchegliakova (1995) studied a section located in the northwestern Middle Magdalena

Valley, where the contact with the underlying La Luna Formation is exposed. She recorded

occurrences of Ammobaculites colombianus and Rugoglobigerina macrocephala, restricting the

age of the formation to the Middle to Upper Maastrichtian. Also, Tchegliakova (1996) analyzed the

Umir and Cimarrona formations in the Honda-Guaduas area, in Southern Middle Magdalena Valley

basin. Foraminiferal assemblages of Middle to Late Maastrichtian planktonic zones Gansserina

gansseri and Abathomphalus mayaroensis were recognized. The Campanian was not recognized

in this section either (Tchegliakova, 1996).

20

19

4. MATERIALS AND METHODS

Eighty samples were collected from a Middle to Upper Umir Formation composite section.

This composite section consists of four cores drilled by Ecocarbón (1996) during a coal exploration

campaign on the western side of the Los Andes syncline, in the Central Eastern MMVB (Figure 6).

The correlation between cores and their stratigraphic position were established using a stratigraphic

framework based on the recognition of coal beds and sandstone levels identified in previous surface

studies (Ecocarbón, 1996; Ortiz and Florez, 1997).

20

Figure 6. Location of the cores PPI-3, PPM-5, PPM-2, and PPM-1 in San Luis Area, Los Andes syncline, Central-Eastern MMVB.

21

Up

per

Um

irM

idd

le U

mir

9.1020.0028.00

38.30

48.0056.00

68.00

84.0087.7099.70108.00

121.70

140.00148.00

161.10

172.00182.00184.00196.00

208.10

220.00

232.00

244.00

Coal bed No. 150

Coal bed No. 270

Coal bed No. 410

Coal bed No. 440

166

150

160

125

100

75

50

25

0(meters)

PPM-10 150

Gamma Log(API)

(meters)

PPM-2

288.5

275

250

225

200

175

150

125

100

75

50

25

130

0 150Gamma Log

(API)

PPM-5

275

250

225

200

175

150

125

100

75

50

25

60(meters)

281.5

0 150Gamma Log

(API)

0 150Gamma Log

(API)(meters)0

25

50

75

100

125

150

175

200

225

250

PPI-3

SSW

2.8 Km. 2.9 Km. 2.0 Km.

NNE

Lagoon Fill

Channel / Crevasse splays

Coal

Facie

s A

sso

cia

tio

n

PPM-5

PPI-3

1040000 1050000

123

0000

1225

000

PPM-2

PPM-1

N

2 Km.

32.00

44.10

56.00

68.8078.45

98.00100.30112.00

125.50

137.00

160.00

172.05

184.15

216.00

230.50

243.00253.00

267.60

280.00

23.5426.0032.7042.0051.9360.0072.25

85.8092.05

104.50115.25124.00133.20143.00152.00160.00

30.00

41.0049.80

63.00

74.70

87.0097.40

109.90

121.50

134.00

146.30

158.00

170.40

182.00

194.40

206.30212.40224.10

236.75

249.05

262.20

273.00

Figure 7. Composite stratigraphic section of the Middle/Upper Umir Formation in the Los Andes syncline, Central-Eastern MMVB, Colombia (modified from Ortiz and Florez, 1998).

22

The stratigraphic position and the intervals covered for each core are shown in figure 7.

The Middle Umir Formation was recovered from Cores PPI-3 (6.3804N; 73,4052W) and PPM-

5 (6.3926N; 73.401W) (Figure 7). These cores were drilled to 261 meters and to 261.60 meters,

respectively. Cores PPM-1 (6.4135N; 73.3947W) and PPM-2 (6,4045N; 73.391W) covered the

Upper-middle to Uppermost Umir Formation, and were drilled to 166 and 288 meters, respectively

(Figure 7). The composite section corresponds to approximately 900 meters of stratigraphic

thickness.

The samples were prepared for palynological content in the Biostratigraphy Laboratory

of the Colombian Petroleum Institute (ICP). The procedure followed the technique described by

Traverse (1988), and involved the initial digestion of 20 grams of sample in hydrochloric (HCl)

and hydrofluoric (HF) acids for dissolving carbonates and silicates, respectively. Heavy liquid

separation was performed using zinc bromide (ZnCl2) to remove residual minerals. A controlled

oxidation was performed on the half portion of the residue in order to disaggregate palynomorphs

from organic debris and clays. The residues were sieved using a 10 µm nylon screen. Two slides,

one oxidized and one non-oxidized were analyzed per sample.

Palynological analyses were conducted using a BX41 Olympus light microscope at the

Center for Excellence in Palynology (CENEX) at Louisiana State University (LSU). A minimum

of 300 grains of spores, pollen, acritarchs and dinoflagellate cysts were tabulated per slide when

possible. Following this step, the rest of the slide was scanned without tabulation in order to scan

potentially rare species. The slides were scanned using a 20x objective and detailed examination

and description of palynomorphs was done under a 60x oil immersion objective.

Species identification was made using formal descriptions and illustrations from specialized

literature (Van der Hammen, 1954; Van der Hammen, 1957; Van der Hammen and García de

Mutis, 1966; Germeraad et al., 1968; Sole de Porta, 1971; Sole de Porta, 1972; Muller et al., 1987;

Sarmiento, 1992; Jaramillo and Dilcher, 2001; Yepes, 2002; Jaramillo and Rueda, 2004; Jaramillo

et al., 2007; Jaramillo et al., 2010; Slimani et al., 2010) and the “Morphological Electronic

23

Database of Cretaceous-Tertiary and Extant pollen and spores from Northern South America” by

Jaramillo et al. (2011). Taxonomic revision was done using the reference palynotheca curated at

the Smithsonian Tropical Research Institute (STRI) in Panama, and in the Colombian Petroleum

Institute (ICP) in Colombia, where holotypes and paratypes of pollen, spores and dinoflagellates

cysts from Northern South America are available.

Distribution and range charts were generated using Stratabugs biostratigraphic data

management software.

24

5. RESULTS

A total of 201 morphotypes were identified and 17,410 palynomorphs were counted. The

morphotypes include 156 species of pollen and spores, 39 species of dinoflagellate cysts, 3 species

of acritarchs, and 3 species of unknown algae. Although palynomorph assemblages consist of

spores, pollen, dinoglagellates cysts, acritarchs, foram linings and other algae, 95% of the recovered

palynomorphs belong to pollen and spore groups, while only 5% includes dinoflagellates cysts,

acritarchs, foram lining and algae. Fungal spores and abundant organic matter were recovered in

all the samples. The recovery was variable but good in general: 80% of the samples, equivalent to

64 slides, were palynologically productive and only 20% of them (16 slides) had a total counting of

palynomorphs below 100 grains. Those samples with low recovery were removed from quantitative

analysis.

% Marine Palynomorphs

% OtherAngiosperms% Spinizonocolpites% Echimonocolpites % Palms% Spores

0.00 0.00 0.00 0.000.00 0.0010.00 10.00 10.00 10.0010.00 10.0020.00 20.00 20.00 20.0020.00 20.0030.00 30.00 30.00 30.0030.0040.00 40.00 40.0050.00 50.0060.00 60.0070.00 70.0080.00 90.00

Up

pe

r U

mir

Mid

dle

Um

ir

0

100

200

300

400

500

600

700

800

Figure 8. Relative abundance of significant palynomorph groups in the composite section for Middle – Upper Umir Formation.

Percentages of significant palynomorphs groups are presented in figure 8. Distribution

charts for each core are given in Appendixes A to D. Generalized quantitative distribution and

range charts for the Umir Formation is included in Appendixes E to F. The palynomorphs taxa

recovered are listed in Appendix G and illustrated in Plates 1–7.

5.1. Palynology of Core PPI-3

Good recovery of palynomorphs and organic matter were found in this section, with the

exception of the interval between 244 and 196 m, at the base of the core, where the total counting

of palynomorphs in slides 196 m, 208.10 m, 232 m and 244 m was below 100 grains (see Appendix

A for details and Figure 9 for summary). Fern spores, including mainly psilate-trilete spores, are

the dominant component in palynological assemblages with a relative abundance ranging from

50% to 80% of the assemblage recovered, followed by Echimonocolpites protofranciscoi (10%

to 30%), Spinizonocolpites group (5% to 12%) and Angiosperm pollen (3% to 10%). Palm pollen

represented by monocolpate grains comprise from 1 to 6 % of the assemblages, while dinoflagellates

cysts range from 2 to 6 % (Figure 9).

The interval between 244 m and 196 m, with low recovery, is characterized by

low relative abundances of Psilatriletes group and Echimonocolpites protofranciscoi along with

Figure 9. Relative abundances of the most abundant palynomorph groups in Core PPI-3.

25

0.00 10.00 20.00


0.00 10.00 20.00

% OtherAngiosperms

0.00 10.00 20.00

% Spinizonocolpites

0.00 10.00 20.00 30.00 40.00

% Echimonocolpites

0.00 10.00

% Palms

9.1

59.1

109.1

159.1

209.1

0.00 10.00 20.00 30.00 40.00 50.00 60.00 70.00 80.00 90.00

% Spores

Mid

dle

Um

ir

26

26

occurrences of Araucariacites australis, Gabonisporis vigorouxii, Muerrigerisporis “ardilenses”,

Neoraistrickia “constrictus” and Crusafontites grandiosus (Appendix A). Angiosperm pollen

reaches 10% of the assemblage and includes occurrences of Echitriporites trianguliformis,

Proxapertites humbertoides, Psilatricolpites josephinae, Retitricolpites josephinae and

Ulmoideipites krempii.

Good recovery was obtained between 184 m and 128 m. This interval is characterized by

high abundances of Psilatriletes group, moderate abudances of Echimonocolpites protofranciscoi

and low relative abundances of Echitriletes “protomulleri”, Gabonisporis vigorouxii and

Retitricolpites josephinae. Buttinia andreevi, Verrutriletes virueloides, Zlivisporis blanensis,

Gemmamonocolpites dispersus, Echitriletes “acanthotriletoides” and Ulmoideipites krempii are

also found within this zone. A spike in spores of Laevigatosporites granulatus identified at 161.1

m constitutes one of the most important biostratigraphic event in this interval (Appendix A).

From 108 m to 9.10 m, high relative abundance of the Psilatriletes group and Echimonocolpites

protofranciscoi dominate the assemblages. Abundances of Spinizonocolpites baculatus and

Spinizonocolpites “brevicolpatus” increase between 121.80 and 99.70 m. Low relative abundance

in Scabratriletes “granularis” and Diporoconia cf. Diporoconia iskaszentgyoergyi occur between

108 and 99.70 m. Arecipites regio, Buttinia andreevi, Crusafontites grandiosus, Echimonocolpites

“pachyexinatus”, Echitriporites trianguliformis, Stephanocolpites costatus and Ulmoideipites

krempii are continuously present in the assemblage from 56 m upwards. Sparse occurrences

of Annutriporites iversenii, Bacumorphomonocolpites tausae, Foveotriletes margaritae and

Monocolpites grandispiniger are also recorded (Appendix A).

The highest abundance in dinoflagellate cysts recovered for core PPI-3 is registered at 48

m. This event include species such as Spiniferites sp., Andalusiella polymorpha, Cerodinium sp.,

Lingulodinium sp. and Senegalinium sp. Other dinoflagellate cysts recorded in this core include

Cordosphaeridium sp., Exochosphaeridium sp., Palaeocystodinium sp. and Florentinia aff.

mantellii. Overall, dinoflagellate cysts exhibit a good preservation.

27

5.2. Palynology of Core PPM-5

Good recovery of palynomorphs was obtained between 280 and 100.3 m except for the

interval between 88 and 32 m, where the recovery was poor. Within this zone, only the slide

at 68.80 m had a total counting higher than 100 grains (see Appendix B for details and Figure

10 for summary). Palynological assemblages are dominated by the Psilatriletes group and

Echimonocolpites protofranciscoi. Relative abundances of these two morphotypes show opposite

tendencies: the percentage of Psilatriletes group increases from 50%, at the base of the core, to

90% at the top, while the percentage of Echimonocolpites protofranciscoi varies from 35% at

the base to 5% at the top (Figure 10). Angiosperm pollen also exhibit the same tendancy, with

decreased abundances upward, from 12% to 5.

In addition to high relative abundances of Psilatriletes group and E. protofranciscoi,

moderate relative abundances of Spinizonocolites baculatus and Araucariacites australis, and low

relative abundances of Proteacidites dehaani and Verutriletes virueloides characterize palynological

assemblages between 280 and 172.05 m. Moderate relative abundances of Psilatricolpites

hammenii were registered between 280 and 230.50, and a spike of Diporoconia cf. Diporoconia

iskaszentgyoergyi was recorded at 243 m. Occurrences of Bacumorphomonocolpites tausae,

Figure 10. Relative abundances of predominant palynomorph groups in Core PPM-5.

% OtherAngiosperms

0.00 10.00 20.00

% Spinizono-colpites

0.00 10.00

% Echimonocolpites

0.00 10.00 20.00 30.00 40.00

% Palms

0.00 10.00 20.00


0.00 10.00 20.00

% Spores

68

118

168

218

268

0.00 10.00 20.00 30.00 40.00 50.00 60.00 70.00 80.00 90.00

Mid

dle

Um

ir

28

Buttinia andreevi, Echitriletes “protomulleri”, Gabonisporis vigorouxii, Periretisyncolpites

giganteus and Retitricolpites josephinae are also observed (Appendix B).

The interval between 160 and 100.30 m is marked by an increase in relative abundances

of the Psilatriletes group and a decrease of Echimonocolpites protofranciscoi. Also decrease

abundances of Spinizonocolpites group and Diporoconia cf. Diporoconia iskaszentgyoergyi are

noted. First occurrences of Arecipites regio, Clavasporites mutisii, Cingulatisporis verrrucatus,

Echimonocolpites “pachyexinatus”, Gemmamonocolpites dispersus, Horniella lunarensis,

Periretisyncolpites magnosagenatus, Proxapertites verrucatus and Retidiporites botulus are

recorded in this interval.

As stated above, only one layer (at 68.8 m) yielded a rich assemblage within the poor-recovery

interval (88 and 32 m). Predominant species recovered include specimens of the Psilatriletes

group along with occurrences of Arecipites sp., Araucariacites australis, Buttinia andreevi, E.

protofranciscoi, Retitricolpites josephinae, Spinizonocolpites baculatus and Ulmoideipites krempii

(Appendix B).

The recovery of dinoflagellate cysts was poor to fair and their distribution scattered. The

assemblage includes occurrences of Andalusiella sp., Andalusiella gabonenesis, Cerodinium

diebelii, Dinogymnium acuminatum, Dinogymnium sp., Exochosphaeridium sp., Fibrocysta sp.,

Glaphyrocysta sp., Senegalinum microspinosum and Spiniferites sp.


Good recovery of palynomorphs was obtained in the intervals 273 to 97.4 m and 41 to

30 m, while the interval between 87 to 49.80 m yielded only a poor assemblage (see Appendix

C for details and Figure 11 for summary). High relative abundances of Psilatriletes group and

Echimonocolpites protofranciscoi again dominate the palynological assemblages. Two spikes of

E. protofranciscoi relative abundances occurred at 206.30 m (54%) and 109.90 m (64 %) (Figure

11). Below the lower spike, between 273 and 212.40 m, high relative abundances of Scabratriletes

granularis and Spinizonocolpites baculatus, and moderate relative abundances of Araucariacites

australis, Echitriporites suescae, Proxapertites humbertoides, Proxapertites operculatus and

Proxapertites verrucatus characterize the interval. Occurrences of Bacumorphomonocolpites

tausae, Buttinia andreevi, Diporoconia cf. Diporoconia iskaszentgyoergyi and Syndemicolpites

typicus are also registered (Appendix C).

Within the interval between 206.30 m and 109.90 m (the two spikes of E. protofranciscoi), the

assemblage is dominated by high relative abundances of the Psilatriletes group and Scabratriletes

granularis and moderate relative abundances of Psilatricolpites hammenii, Scabratriletes

granularis and Spinizonocolpites baculatus.

Poor recovery of palynomorphs was obtained between 87 and 49.80 m. Between 41

and 30 m, the Psilatriletes group and E. protofranciscoi dominate the assemblage. Moderate

relative abundances of the Proxapertites group (P. humbertoides, P. operculatus, P. psilatus,

P. sulcatus, P. verrucatus) including a spike in Proxapertites operculatus at 41 m characterize

this interval. Moderate relative abundances of Echitriporites trianguliformis and occurrences of

Arecipites regio, Colombipollis tropicalis, Monocolpites grandispiniger, Proteacidites dehaani

and Stephanocolpites costatus are also present. In addition to the Psilatriletes group, ferns spores

are also represented by moderate to low abundances of Foveotriletes margaritae, Gabonisporis

vigorouxii, Murrigerisporis ardilensis and Scabratriletes granularis (Appendix C).

The distribution of dinoflagellate cysts was sparse and their preservation was decent. A

29

30

80

130

180

230

0.00 0.0010.00 10.0020.00 20.0030.00 30.0040.00 40.0050.00 50.0060.00 60.0070.00 70.0080.00 90.00

% Marine Palynomorphs0.00 10.00 20.00 0.00 10.00 20.00

% OtherAngiosperms

0.00 10.00 20.00 30.00

% Palms0.00 10.00 20.00

% Spinizono-colpites% Echimonocolpites% Spores

Up

pe

r U

mir


30

spike of dinocysts was identified at 146.30 m with relative abundances making up to 20% of

the assemblage. The association consists of Achomosphaera ramulifera, Achomosphaera sp.,

Cerodinium sp., Spiniferites sp., Hystrichodinium sp. and Phelodinium sp. Between 273 to 158

m, fair to poor recovery of dinoflagellate cysts was registered. The assemblage is characterized

by occurrences of Achomosphaera sp., Andalusiella rhomboides, Andalusiella sp., Areoligera

senonensis, Cerodinium speciosum, Cordosphaeridium sp, Dinogymnium sp., Florentinia mantellii,

Hystrichokolpoma sp., Senegalinium sp. and Spiniferites sp.

Occurrences of Andalusiella gabonensis, Andalusiella sp., Cerodinium speciosum,

Cerodinium sp., Exochosphaeridium sp., Fibrocysta sp., Palaeocystodinium golzowense,

Palaeocystodinium sp., and Senegalinium sp. characterized the assemblage between 97.4 and

30 m. Worth noted is the first occurrence of Manumiella seelandica, a late Maastrichtian global

marker, at 74.70 m (Appendix C).


In general, good recovery of palynomorphs was obtained at this core, except at 160 and

72.25 m, where the recovery was poor. As in the previous cores, high relative abundances of the

Psilatriletes group and Echimonocolpites protofranciscoi dominate palynological assemblages.

This said, the percentages of these two morphotypes are lower at the top of the core, and angiosperm

pollen and dinoflagellate cysts constitute a much important component (Figure 11). The relative

abundance of the Spinizonocolpites group also drops to a maximum of 5%.

Between 152 and 85 m, the Psilatriletes group and E. protofranciscoi are associated with

moderate to low abudances of Araucariacites australis, Echitriporites suescae, Psilatricolpites

hammeni, Retitricolpites josephinae and Scabratriletes granularis. Low relative abundances

of Arecipites regio, Foveotriletes margaritae, Gemmamonocolpites dispersus, Longapertites

proxapertitoides var. proxapertitoides, Syndemicoliptes typicus and Tetradites umirensis are also

tabulated (see Appendix D for details and Figure 12 for summary).

Between 152 and 124 m, dinoflagellate cysts represent 10% of the association (Figure 10).

Dinocysts assemblages consist of Spiniferites sp. and Achomosphaera sp. accompanied by low

numbers of Andalusiella gabonensis, Andalusiella – Palaeocystodinium Complex, Cerodinum sp.

and Florentinia mantellii.

As mentioned above, the percentages of Psilatriletes group and E. protofranciscoi

decreased between 60 and 23.54 m, and are being replaced by angiosperm pollen and dinoflagellate

cyst. Moderate frequencies of Proxapertites group, mostly P. humbertoides and Proxapertites

operculatus are also registered. Low numbers of Proxapertites verrucatus, Proxapertites psilatus,

Proxapertites sulcatus, Colombipollis tropicales, Echitriporites suescae, Retitricolpites josephinae,

Psilatricolpites hammenii, Stephanocolpites costatus and Ulmoideipites krempii are recorded too.

In addition to the Psilatriletes group, fern spores are represented by moderate relative abundances

of Scabratriletes granularis and Foveotriletes margaritae (Appendix D).

Dinoflagellate cysts comprised 20 – 35% of the association in this interval. The sample

taken at 60 m yielded moderate relative abundances of Achomosphaera sp. and Andalusiella

sp. and some Spiniferites sp., Cordosphaeridium sp., Hystrichosphaeridium sp., Areoligera

senonensis, Palaeocystodinium sp., Andalusiella polymorpha, Andalusiella gabonensis and

Cerodinium sp. The assemblage in the sample taken at 51.93 m consists mainly of Gonyaulacacean

cysts. Achomosphaera sp. and Spiniferites sp. dominate the association and occurrences of

Cordosphaeridium sp., Achomosphaera ramulifera, Fibrocysta sp., Hystrichokolpoma bulbosum,

31


% OtherAngiosperms

% Spinizonocolpites% Echimonocolpites % Palms% Spores

23

43

63

83

103

123

143

0.00 0.00 0.000.00 0.00 0.0010.00 10.00 10.0010.00 10.00 10.0020.00 20.00 20.0020.00 20.0030.00 30.00 30.0030.0040.00 40.00 40.0040.0050.00 50.0060.00 60.0070.00 80.00 90.00

Up

per

Um

ir


32

32

Hystrichosphaeridium sp., Lingulodinium sp. and Oligosphaeridium sp. were also registered

(Appendix D). This is interval is not only richer in marine palynomorph, it is also much more

diverse in dinoflagellate species recovered.

The slide taken at 42 m mostly yielded peridinoid cysts such as specimens from the

genera Andalusiella and Palaeocystodinium. A moderate relative abundance of Andalusiella sp.

and Andalusiella polymorpha along with occurrences of Andalusiella gabonensis, Andalusiella

mauthei, Andalusiella rhomoboides, Palaeocystodinium australinum and Cerodinium sp. were

also noted. Specimens of Fibrocysta sp. were also recognized at this level. Again worth noted are

the occurrences of Manumiella seelandica and Alysogiminum euclaense that are also found at this

level (Appendix D).

33

6. DISCUSSION

6.1. Biostratigraphy

Three informal biostratigraphic zones (A to C) are proposed based on the analysis of

qualitative and quantitative biostratigraphic events observed in cores PPI-3, PPM-5, PPM-2 and

PPM-1 (Figure 13). The zones were defined mostly by using changes in palynological assemblages

and abundances, along with a few last or first occurrence data (Appendixes E and F). As is

sometimes the case with biostratigraphic events, it is important to keep in mind that events might

be influenced by environmental and facies changes and these event are thus sometimes regional

in scope and hence cannot be strictly considered as global biostratigraphic events. Since the Umir

Formation recorded a dramatic change in depositional environments from predominantly marine

conditions, in the Campanian, to transitional conditions in the Maastrichtian, the occurrence of

some taxa might have been controlled by changes in facies.

When possible, the zones have been correlated with previous palynological zonations (Van

der Hammen, 1954; Van der Hammen, 1957; Germeraard et al., 1968; Sole de Porta, 1971; Sole

de Porta, 1972; Muller et al., 1987, Sarmiento, 1992) and age determinations have been based

on biostratigraphic events previously reported for Late Cretaceous sections in Northern South

America and Africa (Germeraard et al., 1968; Muller et al., 1987; Sarmiento, 1992; Yepes, 2001;

Pocknall, 2001; Jaramillo and Rueda, 2004; De la Parra, 2009; Slimani et al., 2010), or in global

range charts (e.g., Williams and Bujak, 1985; Williams et al., 1993).

Quantitative distribution and range charts for the composite section are presented in

Appendices E and F, respectively. The zonation developed through this study and the most important

biostratigraphic events are summarized in figure 13. The three zones are described below, from

base to top.

6.1.1 Palynological Zone A

Definition: The top of the zone is defined by the last occurrence of Ariadnasporites sp. and

the first occurrence of Dinogymnium sp. Its base corresponds to the base of the section.

34

Figure 13. Zonation and key biostratigraphic events of the Umir formation, San Luis area, Middle Magdalena Valley Basin (MMVB).

Depth(Com-positeUnits)

50m

100m

150m

200m

250m

300m

350m

400m

450m

500m

550m

600m

650m

700m

750m

800m

850m

Zo

ne Biostratigraphic Events

Zo

ne C

Zo

ne B

Zo

ne A

Last Occurrence of Ariadnaes-porites sp.

First occurrence of Dinogym-nium sp.

First occurrence of Andalusiella polymorpha

First occurrence of Fibrocysta sp.

First occurrence of Andalusiella sp. and Cerodinium speciosum

First occurrence of Psilamono-colpites operculatus

First occurrence of Achomos-paera sp.

Manumiella Seelandica

Syncolporites lisamae

1*

1* Co-ocurrence Hystrichokolpoma bulbosum and Alysogymnium euclaense

Last occurrence of Retistephanocolpites “jandufourioides”

Moderate frequencies of Scabratriletes granularis

Moderate tohigh frequencies of Scabratriletes granularis andSpinizonocolpites Baculatus

Spike of Diporoconia cf. Diporoconia iskaszentgyoergyi

Spike of Achomosphaera sp.and Andalusiella spp.

Spike of Spiniferites sp.

Spike of Echimonocolpitesprotofranciscoi

Continouous record ofFibrocysta sp.

Spike of Proxapertitesoperculatus

Spike of Peridinoid cystsSpike of Achomosphaera sp.

Spike of skolochorate cysts

Spike of Laevigatosporites granulatus

Continuous co-occurrence of Araucariacites australis, Buttinia andreevi, Echitriporites trianguliformis, Retitricolpites josephinae and Ulmoideipites krempii

Moderate frequencies of Spinizonocolpites group

Psiladiporites “operculatus”

Echitriletes “intercolensis”

Moderate frequencies of Proteacidites dehaani,Spinizonocol-pites baculatus andAraucariacites australis

Moderate frequencies of Psilatricolpites hammenii

Moderate frequencies of Psilatricolpites hammenii

Samples

PPM-1 26PPM-1 32.7

PPM-1 42

PPM-1 51.93PPM-1 60

PPM-1 72.25

PPM-1 85.8PPM-1 92.05PPM-1 30PPM-1 104.5PPM-2 41PPM-1 115.25PPM-2 49.8PPM-1 124PPM-2 63PPM-1 133.2PPM-2 74.7PPM-1 143PPM-1 152PPM-2 87PPM-1 160PPM-2 97.4

PPM-2 109.9

PPM-2 121.5

PPM-2 134

PPM-2 146.3

PPM-2 158

PPM-2 170.4

PPM-2 182

PPM-2 194.4

PPM-2 206.3PPM-2 212.4

PPM-2 224.1

PPM-2 236.75

PPM-2 249.05

PPM-2 262.2

PPM-2 273PPM-5 32

PPM-5 44.1

PPM-5 56

PPM-5 68.8

PPM-5 78.45

PPM-5 88

PPM-5 100.3

PPM-5 112

PPM-5 125.5

PPM-5 137

PPM-5 160

PPM-5 172.05

PPM-5 184.15

PPM-5 216

PPM-5 230.5

PPM-5 243

PPM-5 253

PPM-5 267.6

PPM-5 280

PPI-3 9.1

PPI-3 20PPI-3 28

PPI-3 38.3

PPI-3 48PPI-3 56

PPI-3 68

PPI-3 84PPI-3 87.7

PPI-3 99.7PPI-3 108

PPI-3 121.7PPI-3 128

PPI-3 140PPI-3 148

PPI-3 161.1

PPI-3 172

PPI-3 184

PPI-3 196

PPI-3 208.1

PPI-3 220

PPI-3 232

PPI-3 244

Lithostratigraphy

Coal bed No. 440

Coal bed No. 410

Coal bed No. 270

Up

pe

r U

mir

Mid

dle

Um

irU

mir

up

per

san

dsto

nes

35

Characteristics: This zone is dominated by an assemblage of fern spores including high

relative abundances of the Psilatriletes group, along with moderate abundances of Scabratriletes

granularis, Echitriletes “protomulleri” and Gabonisporis vigorouxii, and low abundances of

Verrutriletes virueloides and Verrutriletes “magnovirueloides”. A spike in Laevigatosporites

granulatus was recognized in the lower part of the zone.

High to moderate abundances of Echimonocolpites protofranciscoi and moderate relative

abundances of the Spinizonocolpites group characterize the middle of this section. Occurrences

of Araucariacites australis, Buttinia andreevi, Echitriporites trianguliformis, Retitricolpites

josephinae and Ulmoideipites krempii are common and continuous. Occurrence of dinoflagellate

cysts is sparse but Spiniferites sp., Exochosphaeridium sp. and Senegalinium sp. were recorded in

the lower and middle section.

Stratigraphic position: This zone includes the lower section of the Middle Umir formation

recorded in Core PPI-3 and the first samples of Core PPM-5.

6.1.2 Palynological Zone B

Definition: The base of this zone is marked by the first occurrence of Dinogymnium sp. and

the top of this zone is defined by the first occurrence of Achomosphaera sp.

Characteristics: The last occurrences of Tricolpites “marginobaculatus” and

Echistephanocolpites “minutiechinatus” and the first occurrence of Psilamonocolpites operculatus

are recorded close to the base of the zone. Also, the last appearance of Retistephanocolpites

“jandufouriodes” and the full range of Echitriletes “intercolensis” and Psiladiporites “operculatus”

are restricted to this interval.

In addition to these events, the palynological assemblage is dominated by the Psilatriletes

group and Echimonocolpites protofranciscoi. Moderate relative abundances of Scabratriletes

granularis, Psilatricolpites hammeni and Proteacidites dehaani occurred in the lower part of the

Zone B. A spike in Diporoconia cf. Diporoconia iskaszentgyoergyi was recorded above the base

of the zone.

36

36

As in Zone A, occurrence of dinocysts is sparse, but first occurrences of Fibrocysta sp.,

Cerodinium speciosum, Andalusiella gabonensis and Andalusiella sp. are identified within this

zone.

Stratigraphic position: This zone covered the Upper section of the Middle Umir formation

and its top coincides with the boundary between Middle and Upper Umir established by Ecocarbón

(1996). This zone was recognized in Core PPM-5 and the base of Core PPM-2.

6.1.3 Palynological Zone C

Definition: The base of this zone is defined by the first occurrence of Achomosphaera sp.,

and the top is not defined as it coincides with the top of the studied section.

Characteristics: This zone is characterized at its top by an increase in the occurrence

of dinoflagellate cysts. The first occurrences of Areoligera senonensis, Florentia mantellii,

Hystrichodinium sp. and Andaluseilla rhomboides are recorded at the base of this zone. In the upper

section, the first occurrences of Andalusiella gabonensis, Andalusiella mauthei, Alysogymnium

euclaense, Manumiella seelandica, Hystrichokolpoma bulbosum and Palaeocystodinium

golzowense are also registered. In addition, three spikes in gonyaulacaceaen and peridinoids cysts

are recognized. From base to top, these events were identified as follows: in the lower section, a

spike in Spiniferites sp., Achomosphaera sp., and undifferentiated gonyaulacaceaen dinocysts is

identified; in the upper section, in the top of the Upper Umir sandstones, a spike in Spiniferites

sp. and Achomosphaera sp. along with low abundances in Andalusiella sp. and Hystrichokolpoma

bulbosum, Achomosphaera ramulifera, Hystrichosphaeridium sp., Cordosphaeridium sp. are

recognized; and finally, above the Upper Umir sandstones, a spike in peridinoid cysts including

several species of the genera Andalusiella and Palaecystodinium was recorded. The occurrence of

Manumiella seelandica at the top of the section is important as a late Maastrichtian stratigraphic

marker. Occurrences of Fibrocysta sp. along the Upper Umir Sandstones are also frequent.

In addition to dinoflagellate cyst events, an increase in the numbers of Proxapertites was

also identified. Proxapertites operculatus shows a spike in relative abundance in the middle section

37

of the Upper sandstones, and moderate frequencies of Proxapertites humbertoides were recognized

above the sandstones. Moderate frequencies of Arecipites regio and Echitriporites trianguliformis

were also identified in this interval. At the base of the section high frequencies of Scabratriletes

granularis, Psilatricolpites hammenii and Spinizonocolpites baculatus are significant. Also, the

stratigraphic range of Syncolporites lisamae and Psilabrevitricopites simpliformis is restricted to

this zone.

Stratigraphic position: This zone covered the Upper Umir formation and its Upper section

includes the Upper Umir sandstones. This zone was recognized in Cores PPM-1 and PPM-2.

6.2 Age Assessment and Comparison with Previous Studies

6.2.1 Pollen and Spores Assemblages

Several species considered as important key taxa in previous palynological biostratigraphic

studies of the Late Cretaceous of Northern South America were recorded in Middle – Upper Umir

Formation in the San Luis area (MMVB). The key taxa include: Echimonocolpites protofranciscoi,

Proteacidites dehaani, Buttinia Andreevi, Foveotriletes margaritae, Spinizonocolpites baculatus,

Stephanocolpites costatus, Colombipollis tropicalis, Proxapertites operculatus, Proxapertites

humbertoides, Duplotriporites ariani and Araucariacites australis. Other taxa previously

restricted to the Paleocene, including Proxapertites psilatus, Syncolporites lisamae, Longapertites

vaneendenburgi, Psilabrevitricolporites annulatus and Zonotricolpites variabilis (Samiento, 1992)

were also registered in the Umir Formation. Proteacidites dehaani was recovered throughout the

entire studied section showing low numbers but a continuous record. Germeraard et al. (1968) used

this taxa and its co-occurrence with high abundances in Foveotriletes margaritae to characterize

the Maastrichtian in tropical areas. In the Umir formation in MMVB, occurrences of F. margaritae

associated with P. dehaani are also believed to mark the same stratigraphic level. According to

Germeraard et al. (1968), the last occurrence of P. dehaani marks the K/T boundary. Hence the

co-occurrence of these two species is used to restrict the age of the interval analyzed to the Late

Maastrichtian.

37 38

Muller et al. (1987) also used the range of P. dehaani to define Zone 13 Proteacidites

dehaani, a Late Maastrichtian zone defined for Colombia and Northwestern Venezuela. According

to Muller´s zonation, this zone is also marked by the first appearance of Foveotriletes margaritae,

Stephanocolpites costatus, Spinizonocolpites spp. and Ulmoideipites spp. The last occurrence of

Buttinia andreevi, Proteacidites dehaani and Aquillapollenites sp. at the top of the zone indicate the

Cretaceous – Tertiary boundary (Muller et al. 1987). In the Umir formation (MMVB), all these taxa

(except for Aquillapollenites sp. that exhibits a sparse recovery) are present throughout the studied

interval. When comparing the results from this study to Muller´s events, a Late Maastrichtian age

is also confirmed for the Umir in MMVB.

Moderate frequencies of Spinizonocolpites baculatus were recorded throughout the Umir

Formation in the San Luis area. The first occurrence of Spinizonocolpites baculatus is mostly

known as a marker for the base of the Paleocene, restricted to the early Cenozoic (Muller et al.,

1987). The results of this study are in disagreement with this general view, but they concur with

the report of minor frequencies of Spinizonocolpites baculatus as early as the Lower Maastrichtian

of Western Venezuela (Pocknall et al. 2001).

High to moderate frequencies of Echimonocolpites protofranciscoi and a continuous record

of Buttinia andreevi were identified throughout the Umir Formation in the San Luis area, with

spikes in abundance of E. protofranciscoi in Zones B and C (Upper Umir). In the Eastern Cordillera,

Sarmiento (1992) recognized both Echimonocolpites protofranciscoi and Buttinia andreevi as

abundant in the Maastrichtian (Zone I Buttinia andreevi) with occasional occurrences in Zone II

Foveotriletes margaritae dated as Paleocene (Sarmiento, 1992). However, as it will be explained

below, Paleocene zones IIA and IIB of Sarmiento (1992) actually correspond to the Maastrichtian.

In the Cesar-Rancheria basin (Northern Colombia) Echimonocolpites protofranciscoi, Buttinia

andreevi and Protecidites dehaani became extinct at the K/T boundary, restricting these species to

the Cretaceous (De la Parra, 2009).

The palynological assemblages in the Umir Formation are very similar to those recorded

by Sarmiento (1992) in the Guaduas Formation (Eastern Cordillera, Colombia). The Maastrichtian

39

Zone I Buttinia andreevi (Sarmiento, 1992) was defined by the high abundance of Psilatriletes

guaduensis and Psilamonocolpites medius and occurrences of Buttinia andreevi, Echimonocolpites

protofranciscoi, Proxapertites humbertoides, Bacumorphomonocolpites tausae, Annutriporites

iversenii, Retidiporites magdalenensis, Stephanocolpites guaduensis, and Retitricolpites

josephinae (Sarmiento, 1992). Taxa restricted to this zone include Retimonocolpites claris,

Crusafontites grandiosus, and Clavatriletes mutisii (Sarmiento, 1992). In the Umir Formation in

MMVB, the palynological assemblages are dominated by the Psilatriletes group, Crusafontites

grandiosus, Clavatriletes mutisii, Annutriporites iversenii, Proxapertites humbertoides and

Bacumorphomonocolpites tausae. As is the case for B. andreevi, E. protofranciscoi and P. dehaani,

the stratigraphic range of these taxa in the San Luis section (MMVB) is wide and corresponds to

the entire interval analyzed. The only difference in the assemblages is the presence of P. dehaani

in the Umir Formation that was not recognized as a taxon present in Zone I Buttinia andreevi of

Sarmiento (1992).

Sarmiento (1992) proposed the Zone II Foveotriletes margaritae (including subzones IIA

and IIb) for the Upper Guaduas Formation (Eastern Cordillera) and assigned a relative age of

Danian to this interval. The Subzone IIA was characterized by the first occurrence of several

species including Foveotriletes margaritae, Longapertites vaneendenburgi, Proxapertites

operculatus, Proxapertites verrucatus, Proxapertites psilatus, Gemmamonocolpites dispersus,

Syndemicolpites typicus, Psilabrevitricolporites annulatus and Zonotricolpites variabilis. The top

was established using the last occurrences of Duplotriporites ariani, Bacumorphomonocolpites

tausae, Araucariacites australis and Zlivisporis blanensis. In the Umir formation in MMVB, F.

margaritae, L. vaneendenburgi, P. operculatus, P. verrucatus, P. psilatus, G. dispersus, S. typicus

and P. annulatus were recorded co-occurring with B. andreevi, E. protofranciscoi and P. dehaani

that are restricted to the Maastrichtian, and with Crusafontites grandiosus and Clavatriletes

mutisii that according to Sarmiento (1992) are restricted to his Maastrichtian Zone I. Then, the

first occurrences used by Sarmiento (1992) for defining the Paleocene Subzone IIA should be

reconsidered as being of Late Maastrichtian age.

39 40

The definition and age of subzone IIB Syncolporites lisamae (Sarmiento, 1992) is controversial

too. Sarmiento (1992) used the first occurrence of Syncolporites lisamae for determining the base

of the zone and reported occurrences of Foveotriletes margaritae, Echitriporites trianguliformis

and Gemmamonocolpites dispersus. In the Umir Formation in MMVB, the first occurrence and

the stratigraphic range of Syncolporites lisamae was recorded only in Zone C of the Upper Umir

Formation. At this interval, the assemblage includes occurrences of F. margaritae, E. trianguliformis

and G. dispersus (as in Sarmiento´s zone) but also B. andreevi, E. protofranciscoi and P. dehaani,

which are all key Maastrichtian markers (Germeraard et al., 1968; Muller et al., 1987; De la Parra,

2009) and Crusafontites grandiosus and Clavatriletes mutisii that according to Sarmiento (1992)

are restricted to the Maastrichtian too. Hence, Sarmiento´s subzone IIB Syncolporites lisamae

should also be re-evaluated and assigned a Late Maastrichtian age.

6.2.2 Dinoflagellate Cysts Assemblages

Several dinoflagellate cysts recorded in the studied section have a first global occurrence

in the Latest Campanian or close to the Campanian-Maastrichtian boundary. Genus Andalusiella,

Palaeocystodinum and Senegalinium have their first appearances in the Uppermost Campanian

(Williams et al., 1993), the Upper Campanian (Willliams and Bujack, 1985) and the Latest

Campanian (Williams et al., 1993), respectively. In the Umir Formation, the first occurrence of

Senegalinium sp. was recorded in core PPI-3 at 244 m, corresponding to the base of the studied

section. Palaeocystodinium sp. was registered by the first time in core PPI-3 at 184 m (Zone A,

lower section of the Middle Umir Formation), and the lowest occurrence of the genus Andalusiella

(first appearance of A. polymorpha) was recorded in core PPI-3 at 48 m. On this basis, an age no

older than Latest Campanian is assigned for the Middle member of the Formation. However, in the

Rio Loro section in Western Venezuela, Pocknall et al. (2001) using graphic correlation established

that the first occurrence of Andalusiella polymorpha in Northern South America is restricted to the

Late Maastrichtian. Other taxa of global significance for the Latest Campanian recognized in the

Umir Formation are the FADs of Cerodinium diebelii (Lentin and Williams, 1980; Williams and

41

Bujak, 1985) found in core PPM-5 at 137 m and of Areoligera senonensis (Williams et al., 1993)

found in core PPM-2 at 224.1 m. These species are recorded through the Maastrichtian up to the

K/T boundary.

The first occurrence of Manumiella seelandica in core PPM-2 at 74.7 m and low

numbers of the same taxa registered in core PPM-1 at 26 m restrict the age of the upper section of

the Umir Formation to the Latest Maastrichtian. The first occurrence of Manumiella seelandica is

a global event that has been used for identifying the Latest Maastrichtian in several areas (Slimani

et al, 2010). In sections located in Northern Colombia and Western Venezuela, Yepes (2001) found

M. seelandica associated to Disphaerogena carpsophaeropsis and Glaphyrocysta perforata just

below the Maastrichtian – Danian boundary. Spike abundances of this species below the K/T

boundary has been also reported in Georgia (Firth, 1987), in the Mediterranean regions (Habib and

Saeedi, 2007), in Ghana (Oboh-Ikuenobe et al., 1998) and in Morocco (Slimani et al., 2010).

The first occurrences of Cerodinium speciosum and Hystrichokolpoma bulbosum, recorded

in core PPM-5 at 172.05 m (middle section Zone B) m and in core PPM-1 32.7 (Top Zone C)

also support a Late Maastrichtian age for the Middle and Upper Umir Formations. These two

events were recognized by Slimani et al. (2010) in the Late Maastrichtian of Morocco and have

been recognized in the Northern Hemispheres in sections calibrated using bellemnite zones and

planktonic foraminifer Globotruncana gansseri zone (Aurisano, 1989; Slimani et al., 2010).

To summarize, dinoflagellate cyst assemblages in the Umir Formation restrict the Middle

member to the Late Maastrichtian and the Upper Member to the Latest Maastrichtian. These results

are in agreement with the age proposed by Tchegliakova (1995) using foraminiferal assemblages of

the planktonic zones Gansserina gansseri and Abathomphalus mayaroensis for the northwestern

Middle Magdalena Valley Basin.

Table 2 presents the ages assigned to zones A, B and C and their probable correlation with

previous studies.

42

6.3 Paleoenvironmental Interpretation

Pollen, spores and dinoflagellate cysts recovered from the Middle – Upper Umir Formation were

grouped in five categories in order to conduct a palaeoenvironmental interpretation. The five

categories defined using the known taxonomic affinity of some taxa and morphological features,

include spores, palms, Spinizonocolpites, marine palynomorphs and “other angiosperms” groups.

The relative abundance of each group in each sample was expressed in percentages, and changes in

these values were used to determine the most probable depositional environment for the formation

(figure 14). The species and genera included in each group are shown in table 3.

Table 2. Comparison between the informal zones proposed for the Late Maastrictian in the Umir Formation and previous Late Cretaceous zonation developed for Northern South America (Modified from Poknall et al., 2001).

43

The spore group is the most abundant component of the palynological assemblages in Umir

Formation. Its relative abundance ranges from 60%-90% in the Middle Umir formation to 30%-

70% in the Upper member, where three spikes in the lower - middle section reach the 90% (Figure

14). This group includes fern spores, with Psilatriletes group as the most abundant, accompanied

by Foveotriletes margaritae, Scabratriletes “granularis”, Gabonisporis vigorouxii and species

from genera Echitriletes and Verrutriletes, among others (Table 3).

The abundance and dominance of Psilatriletes group in the Maastrichtian in Colombia has

been also recorded in the Guaduas Formation (Eastern Cordillera), where their occurrence was

interpreted as indicative of coastal swamps (Sarmiento, 1992; 1994). Fern spores have been also

Table 3. Significant palynomorph groups used in the paleoenvironmental interpretation. Species represented by a single specimen (singletons) were removed from the analysis.

44

considered as an abundant component in coastal pollen assemblages where erosion and transport

are dominant, because they are transported by rivers from coastal swamps and inland forests (Rull,

2000; 2002).

Palms group is the second most abundant component of the palynological assemblages

in the Umir Formation. Its abundance is variable along the studied section: ranging from 10% to

40% in the lower section of the Middle Umir Formation; from 10% to 20% in the upper section of

the Middle member; and reaching 40% - 60% in some spikes located in the Upper member of the

formation (Figure 14). The dominant species in this group is Echimonocolpites protofranciscoi,

Figure 14. Paleoenvironmental interpretation of the Umir Formation (Central Eastern MMVB) based on the relative abundance (expressed in percentages) of significant palynomorph groups.


% OtherAngiosperms

% Spinizono-colpites% Spores

0.00 0.00 0.000.0010.00 10.00 10.0010.0020.00 20.00 20.0020.0030.00 30.00 30.0040.00 40.0050.00 60.00 70.00 80.00 90.00

% Palms

0.00 10.00 20.00 30.00 40.00 50.00 60.00 70.00

Up

per

Um

irM

idd

le U

mir

Lag

oo

nal en

vir

on

men

t, w

ith

co

asta

l sw

am

ps a

nd

estu

ari

ne c

on

dit

ion

sS

em

i-re

str

icte

d b

ay w

ith

str

on

g r

iver

infl

ux

45

but psilate monocolpate grains from genera Arecipites, Monocolpites, Monocolpopollenites,

Psilamonocolpites, Cycadopites are also included; along with monocolpate grains from

genera such as Echimonocolpites, Gemmamonocolpites, Longapertites, Retimonocolpites and

Rugomonocolpites (Table 3). Diporoconia cf. Diporoconia iszkaszentgyoergyi was also included

in this group as it is considered as a palm pollen (Frederiksen et al. 1985).

Palm pollen was recognized as abundant in previous studies in the Umir Formation (Van der

Hammen, 1954; 1957); and in the Guaduas Formation (Eastern Cordillera), where its occurrence

was associated mainly with tidal swamps and alluvial plains (Sarmiento, 1992; 1994). According

to Rull (2000; 2002), palms are an important component in coastal environments due to their

ability to colonize bar sands and prograding sand deposits.

Spinizonocolpites group represents the homonymous genus and includes three different

species, the most common being Spinizonocolpites baculatus (Table 3). Although its relative

abundance was low, ranging from 2% to 10%, the group was frequent and its record was continuous

through the studied section (Figure 14). Spinizonocolpites genus has been taxonomically related

to current mangrove palm Nypa (Germeraard et al., 1968; Rull, 1998), the only palm present in

mangrove ecosystems that nowadays is restricted to estuarine areas and coastlines of Southern

Asia (Germeraard et al., 1968; Rull, 1998). Considered as representative of mangrove pollen,

Spinizonocolpites genus evidences estuarine conditions with a high sea level and wetter conditions

(Rull, 2000; 2002).

Marine palynomorphs group consists of dinoflagellate cysts, acritarchs and foram

linings (Table 3). Its distribution along the Umir Formation was very similar to the record of

Spinizonocolpites genus, and was frequent and continuous through the section. The relative

abundance of this group was low in the Middle Umir Formation ranging between 2%-6% with a

spike equivalent to 10% in the lower section (Figure 14). The Upper Umir formation recorded an

increase in the relative abundance of dinoflagellate cysts, changing from 10% in the lower section,

and reaching 30% to 40% of the assemblages in the top of the section, where the Upper Umir

sandstones are located (Figure 14).

46

Two different categories of dinoflagellate cysts were distinguished in the upper interval of

the Upper Umir formation: the peridinoid group consisting of Andalusiella, Palaeocystodinium,

Senegalinium, Cerodinium, Lejeunecysta and Manumiella genera; and the Spiniferites -

Achomosphaera group, that includes morphotypes from these two genera. Although these

categories were defined using morphological criteria, they probably reflect distinctive ecological

conditions (Yepes, 2001).

Peridinoid cysts are considered to be produced essentially by heterotrophic dinoflagellates

(Harland, 1988; Schioler et al., 1997; Yepes, 2001). These cysts occur in large numbers in Cenozoic

assemblages where diatoms are also abundant (Powell et al., 1990). Hence, they have been used as

indicators of high paleoproductivity related either to upwelling currents (Powell, 1990; Brinkuis,

1994; Eshet et al., 1994) or to river mouths (Brinkhuis, 1984) and river runoff (Yepes, 2001).

In the Maastrichtian of Northern Colombia and Western Venezuela, Yepes (2001) recognized

a marked dominance of peridinoid cysts in the Colón Formation, where this group constituted

approximately 80-100% of the dinocyst assemblages in some intervals. Because of the lack of

sedimentological evidence for upwelling currents, Yepes (2001) suggested a high continental

nutrient supply and closeness to a deltaic system to explain their abundance.

In the Umir Formation, peridinoid cysts constitute 30%-40% of the palynological

assemblages (Figure 14), but they are the dominant component of the dinocyst associations in

the uppermost section. The difference with respect to the values recorded by Yepes (2001) may

be explained by the geographic position of the MMVB in constrast to Yepes´ sections, and the

Maastrichtian paleogeography proposed by Villamil (1999) for Colombia and Western Venezuela.

According to Villamil (1999), a marine seaway oriented in a NE-SW direction covered the Middle

Magdalena Valley Basin and the western foothills of the Eastern Cordillera, in the South, and the

Catatumbo and the Maracaibo Basins in the North during the Maastrichtian. The most distal facies

were deposited in the north and west, where the sections studied by Yepes (2001) (Río Molino and

Río Loro sections) are located. Because MMVB is located in the south, closer to continental areas,

a lower marine influence is expected to be highlighted in the palynological record of MMVB.

47

As in Northern Colombia and Western Venezuela, the abundance of peridinoid cysts in

the Umir Formation seems to be related with intense river influx and high nutrient supply derived

from the continent. In MMVB, there is no evidence of upwelling systems either, but there is

evidence of intense tectonic activity provided by the upward-coarsening lithology of the Umir

Formation, and recorded in the intra-formational conglomerates and the cross-stratified sandstones

located in the Upper Umir member. The Maastrichtian tectonism in the basin is associated with

the accretion of the Western Cordillera in the Early Maastrichtian that caused the initial uplifting

of the Central Cordillera (Gomez et al. 2005). This event also triggered an abrupt change in the

depositional environments where conditions predominantly marine became transitional for the

Latest Cretaceous – Paleocene (Cooper et al., 1995; Villamil, 1999; Gómez et al., 2003; Gómez et

al., 2005). The effects of this event also include the withdrawal of the sea in a northward direction

(Villamil, 1999) and the decrease in the accommodation space (Cooper et al., 1995; Ortiz and

Flórez, 1997; Villamil, 1999; Gómez et al., 2003; Gómez et al., 2005).

The second abundant group of dinoflagellate cysts recorded in the Umir Formation is the

Spiniferites - Achomosphaera complex that includes species of Spiniferites and Achomosphaera

genera. Although the abundance of this group increases in the Upper member of the Umir formation,

using these genera to infer environmental conditions is complex since both of them could occur

either in offshore or transitional environments. Besides, the taxonomic identification of the taxa

belonging to this group was usually possible only to the genus level and that prevent using them

for environmental interpretations. In this study, it is considered that their occurrence evidence

marine influence and brackish conditions during the deposition of the Umir Formation.

The last category interpreted is the “other angiosperms” group that includes tricolpate,

triporate, tricolporate, stephanocolpate, stephanocolporate and pantoporate grains produced in

coastal forests (Sarmiento, 1992), open forests and inland (Rull, 1997; 2002) (Table 3). The relative

abundance of this group is continuous and constant in the Middle Umir Formation, ranging from

2% to 10% (Figure 14). In the Upper member, the abundance of this component increases up to

20% of the assemblages. The increment in the abundance of this group may be associated with the

47 48

intense fluvial transport of sediments evidenced by the Upper Umir sandstones and the abundance

of peridinacean cysts. Since the morphotypes included in this group are related to open forests and

the inland, their occurrence and increase could be linked to an increase in fluvial transportation.

According to Rull (1997) pollen derived from inland vegetation and mountain communities is

abundant in coastal sediments when the sea level is low and erosion and transport are present.

Finally, considering the relative abundance of each category, their distribution along the

Umir Formation and their environmental implications; and also, considering sedimentological

interpretations by Ortiz and Flórez (1997), it is proposed that the formations were deposited

within a lagoonal environment, with coastal swamps and estuarine conditions for the Middle

Umir Formation. The environment for the Upper Umir member probably corresponds to a semi-

restricted bay with strong river influx in the zone close to the coastline (Figure 14).

6.4 Palynological Record of the Umir Formation and the Global Setting

During the Cretaceous period occurred one major evolutionary event: gymnosperms

(including conifers and cycadeoids) that were the dominant component of the vegetation during

the earliest part of the Mesozoic, were rapidly replaced by angiosperms (Figure 15). During this

event named the “Cretaceous Terrestrial Revolution” (Lloyd et al., 2008), all gymnosperm groups

experienced decline, but podocarpoid and araucarioid conifers were more dramatically affected

(Peralta and Falcon, 2012) (Figure 15). The decline of these two conifer groups correlates with a

notable increase in the occurrence of angiosperms that changed from 32% in the Campanian to

78% in the Maastrichtian (Peralta and Falcon, 2012) (Figure 16a).

In the Umir Formation, angiosperms are by far the dominant component of the pollen

assemblages and gymnosperms are only a minor constituent. Angiosperms, represented by 106

species, constitute 80%-90% of the pollen assemblages in the Middle Member (assigned to the

Late Maastrichtian), and 90%-100% of the associations in the Upper Umir Formation (assigned

to the Latest Maastrichtian) (Figure 16b). Gymnosperms, represented only by three species, are

dominated by Araucariacites australis (a pollen grain derived from a gymnosperm belonging to

49

the Araucarioid group), and they showed a continuous but decreasing record along the formation.

In the Middle Umir, gymnosperms constitute up to 18 % of the pollen grains, decreasing upward.

In the Upper Umir Formation, they represent 10% of the associations at the base, and only 1%-2%

at the top (Figure 16b).

Figure 16 shows a comparison between the changes in percentage of abundance for

gymnosperms and angiosperms estimated by Peralta and Falcon (2012) and the changes in

percentage of abundance for gymnosperms and angiosperms in the Late Maastrichtian Umir

Formation, Central-Eastern Middle Magdalena Valley Basin (Figures 16a and 16b, respectively).

Although Peralta and Falcon (2012) calculated the changes in percentage using global data from a

fossil wood database, and in this study the changes were estimated using pollen assemblages from

one site in the Neotropics, there is a strong correspondence in the proportion of gymnosperms

and angiosperms during the Maastrichtian: in both graphs, gymnosperm abundance correspond to

10%-15% approximately, and angiosperm abundance are above the 80% (Figures 16a and 16b).

The dominance of Araucariacites australis (pollen grain produced by an araucarioid

conifer) in the gymnosperm group of the Umir Formation and its decline could be explained if

we consider the general distribution of araucarioids during the Cretaceous and their co-occurrence

with the initial angiosperms. Araucarioids and podocarpoids were the most abundant gymnosperms

constituting 40.1% of all the associations (Peralta and Falcon, 2012). They were globally

distributed from 80°N to 80°S, but they were specially concentrated in tropical and paratropical

belts while they had low records in temperate zones (Peralta and Falcon, 2012)(Figure 15). In

their initial stage, angiosperms occurred mainly in humid tropical and subtropical areas that used

to be dominated by araucarioids (Peralta and Falcon, 2012). Since the appearance and rise of the

angiosperms is considered the main cause of the decline of the gymnosperms, it makes sense

that araucarioids were the group of gymnosperms most affected by the radiation of the flowering

plants as is recorded in the Late Maastrichtian Umir Formation, deposited in the tropical areas of

Northern Western South America.

50

49 50

6.4.1 Dinoflagellate Cyst Assemblages from Umir Formation and Late Cretaceous

Provincialism

Dinoflagellate cyst assemblages identified in the Umir Formation in Central Eastern Middle

Magdalena Valley Basin reflect the Campanian - Maastrichtian provincialism of peridinacean cysts

as recognized by Lentin and Williams (1980).

Based on the latitudinal distribution of peridinacean cysts, Lentin and Williams (1980)

Figure 15 Paleogeographic distribution of Cretaceous conifers and angiosperms based on a fossil wood database (from Peralta and Falcon, 2012).

Be

rria

sia

n–

Ha

ute

riv

ian

(1

45

.5–

12

5 M

a)

Ap

tia

n–

Alb

ian

(1

26

–9

8 M

a)

Ce

no

ma

nia

n–

Sa

nto

nia

n

(99

–8

3 M

a)

Ca

mp

an

ian

-M

aa

str

ich

tia

n

(84

–6

5.5

Ma

)

51

defined three distinctive suites or provinces: the Malloy suite (tropical to subtropical province),

the Williams suite (temperate province) and the McIntyre suite (boreal province). The Malloy

suite was characterized by the co-occurrence of genera Andalusiella, Cerodinium, Lejeunecysta

52

0.00

10.00

20.00

30.00

40.00

50.00

60.00

70.00

80.00

90.00

100.00

Late Maastrichtian Latest Maastrichtian

Rela

tive a

bu

nd

an

ce in

P

ollen

asso

cia

tio

n (

%)

a)

Berriasian–Hauterivian

Aptian–Albian Cenomanian–Santonian

Campanian-Maastrichtian

b)

Figure 16. a) Changes in relative abundance (%) of major Cretaceous conifer and angiosperm groups using fossil wood data (from Peralta and Falcon, 2012). b) Changes in relative abundance (%) of gymnosperms and angiosperms based on pollen data from the Late Maastrichtian Umir Formation, Central-Eastern Middle Magdalena Valley Basin (this study).

51 52

and Senegalinium using data from Spain, Senegal, Brazil and Venezuela. The distribution of this

assemblage restricted the Malloy suite to tropical to subtropical paleolatitudes. The Williams suite

was defined using the occurrence of species of Alterbidinium, Chantagiella (the smaller taxa),

Isabelidinium, Spinidinium and Trithyrodinium. This assemblage, restricted to temperate areas,

was recognized in the Scotian Shelf-Grand banks, offshore eastern USA, southern England and

France. Finally, the McIntyre suite, characterized by species of Chantagiella (the larger taxa) and

Laciniadinium, was recorded in sections in Arctic Canada, the Mackenzie delta, Saskatchewan,

Alberta, South Dakota and Wyoming. The McIntyre suite represents boreal assemblages reflecting

cool temperate conditions (Lentin and Williams, 1980). Although this provincialism was initially

recorded in the Campanian, several studies in the Maastrichtian recognized the same distribution

of peridinacean cyst (Firth, 1987; Oboh-Ikuenobe et al., 1998; Yepes, 2001; Slimani et al, 2011)

In the Umir Formation, peridinacean cyst assemblages are characterized by the dominance

of Andalusiella and Palaeocystodinium genera accompanied by common occurrences of

Senegalinium, Cerodinium and Lejeunecysta genera. This association places the Umir formation

dinocyst assemblages into the tropical to subtropical Malloy suite described by Lentin and Williams

(1980), evidencing presence of tropical warm waters during the Late Maastrichtian in MMVB.

In Northern Colombia (Río Molino section) and Western Venezuela (Río Loro section),

similar dinocyst assemblages belonging to the Malloy Suite were reported in the Maastrichtian

Colón and Mito-Juan Formations by Yepes (2001).

53

7. CONCLUSIONS

Pollen and spore assemblages identified in the Middle-Upper Umir formation, in Central

Eastern MMVB, provided a Late Maastrichtian age for the formation. Global dinoflagellate cyst

events, including the occurrence of Manumiella seelandica at the top of the section, restrict the

upper member to the Latest Maastrichtian, in a time interval that is directly preceding the K/T

boundary.

Comparison with previous studies showed similarities with the regional biostratigraphic

framework (Germeraard et al., 1968; Muller et al., 1987), but also highlighted some differences with

local studies conducted in the Eastern Cordillera (Sarmiento, 1992). Specifically, biostratigraphic

events used to define pollen zones assigned to the Danian in the Eastern Cordillera were recorded

in the Late Maastrichtian in MMVB. Hence, a revision of the zonation proposed by Sarmiento

(1992) is necessary.

Three informal zones (A-C) are proposed using last and first occurrence data and relative

abundance. These zones provide a detailed biostratigraphic control for the entire formation. Zone

A is marked by the predominance of fern spores and covers the Middle Umir Formation. Zones

B and C are marked by higher abundances in dinoflagellate cysts and an increase in angiosperms

abundance, and cover the Upper member.

Important biostratigraphic events including spikes of peridinoid cysts (Andalusiella and

Palaecosytodinium genera), skolochorate cysts (mainly Achomosphaera –Spiniferites complex)

and pollen from Echimonocolpites protofranciscoi and Proxapertites genus were identified at the

top of Zone C in the Upper Umir sandstones. These events, which characterize layers below,

within and above the sandstones, are recognized for the first time in the Umir Formation and in

the MMVB. They have a high potential to assist intrabasinal correlations when evaluating lateral

continuity of this new petroleum target.

Considering the relative abundance of pollen, spores and dinoflagellate cysts, their

distribution along the formation and their environmental implications, the Middle Umir formation

is believed to have been deposited within a lagoonal environment with coastal swamps and

54

53 54

estuarine conditions; while a semi-restricted bay with strong river influx in the zone close to the

coastline must have existed during the deposition of the Upper member.

In the Umir Formation, angiosperms are represented by 106 species and they are by far

the dominant component of the pollen assemblages, making up to 80% - 99% of the associations.

Gymnosperms, represented only by 3 species and dominated by Araucariacites australis, are a

minor component and show a decline in their abundance, from 18 % at the base of the section to

only 1%-2% at the top. The dominant and increasing abundance of the angiosperm pollen, and

the decreasing and subordinate role of the gymnosperms, reflect the global replacement of the

gymnosperms by the angiosperms.

Peridinacean dinocyst assemblages identified in the Umir Formation in MMVB reflect

the Campanian - Maastrichtian provincialism of peridinacean cysts recognized worldwide. The

association characterized by the dominance of Andalusiella and Palaeocystodinium genera

accompanied by common occurrences of Senegalinium, Cerodinium and Lejeunecysta genera

locates Umir Formation assemblages into the tropical to subtropical Malloy suite proposed by

Lentin and Williams (1980).

55

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60

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61

60 61

APPENDIX A QUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN CORE PPI-3 (MIDDLE UMIR

FORMATION) EXPRESSED IN ABSOLUTE ABUNDANCES

Depth

50m

100m

150m

200m

250m

Samples

Sam

ple

sin

Dis

ciplin

e(s

):

Paly

9.10

20.00

28.00

38.30

48.00

56.00

68.00

84.0087.70

99.70

108.00

121.70

128.00

140.00

148.00

161.10

172.00

184.00

196.00

208.10

220.00

232.00

244.00

Absolute abundance (40mm=250 counts)

Ara

uca

ria

cite

sa

ust

ralis

Are

cip

ites

reg

ioD

ipo

roco

nia

cfD

ipo

roco

nia

iszk

asz

en

tgyo

erg

yiE

chim

on

oco

lpite

s"p

ach

yexi

na

tus"

Ech

imo

no

colp

ites

pro

tofr

an

cisc

oi

Ech

itrile

tes

"aca

nth

otr

ileto

ide

s"E

chitr

ilete

s"p

roto

mu

elle

ri"E

chitr

ipo

rite

ssu

esc

ae

Ech

itrip

ori

tes

tria

ng

ulif

orm

isH

am

ula

tisp

ori

sca

pe

ratu

s*1 L

on

ga

pe

rtite

sp

roxa

pe

rtito

ide

sva

rre

ticu

loid

es

Mo

no

colp

op

olle

nite

ssp

.P

rote

aci

dite

sd

eh

aa

ni

Pro

xap

ert

ites

verr

uca

tus

Psi

latr

ico

lpo

rite

s"m

inim

us"

Psi

latr

ilete

sg

rou

p

Re

tipo

llen

ites

"afr

op

olle

nsi

s"R

etis

tep

ha

no

colp

ites

sp.

Re

titri

colp

ites

jose

ph

ina

eS

cab

ratr

ilete

sg

ran

ula

ris

Sp

iniz

on

oco

lpite

sb

acu

latu

sS

pin

izo

no

colp

ites

"bre

vib

acu

latu

s"S

tep

ha

no

colp

ites

cost

atu

sV

err

utr

ilete

s"m

ag

no

viru

elo

ide

s"V

err

utr

ilete

svi

rue

loid

es

Bu

ttin

iaa

nd

ree

viF

ove

op

olle

nite

s"p

erf

ora

tus"

Ga

bo

nis

po

ris

vig

oro

uxi

iL

ae

vig

ato

spo

rite

sg

ran

ula

tus

Psi

lab

revi

tric

olp

ori

tes

an

nu

latu

sP

sila

tric

olp

ites

"min

imu

s"R

etid

ipo

rite

sm

ag

da

len

en

sis

Re

titri

colp

ites

"op

erc

ulo

esp

on

josu

s"R

etit

rip

ori

tes

sp.

Sp

iniz

on

oco

lpite

s"c

lava

tus"

Ulm

oid

eip

ites

kre

mp

iiZ

livis

po

ris

bla

ne

nsi

sC

rusa

fon

tite

sg

ran

dio

sus

Mo

no

colp

ites

gra

nd

isp

inig

er

Pro

xap

ert

ites

hu

mb

ert

oid

es

Pro

xap

ert

ites

psi

latu

sTe

tra

dite

su

mir

en

sis

Ba

cum

orp

ho

mo

no

colp

ites

tau

sae

Ep

he

dri

pite

ssp

.P

sila

tric

olp

ites

ha

mm

en

iiP

sila

trip

ori

tes

sp.

Re

titri

po

rite

s"c

rass

ore

ticu

latu

s"S

ynd

em

ico

lpite

sty

pic

us

Tri

colp

ites

"ma

rgin

ob

acu

latu

s"C

olo

mb

ipo

llis

tro

pic

alis

Ge

mm

am

on

oco

lpite

sd

isp

ers

us

Lo

ng

ap

ert

ites

van

ee

nd

en

bu

rgi

Mu

err

ige

risp

ori

s"a

rdile

nsi

s"N

eo

rais

tric

kia

"co

nst

rict

us"

Pe

rire

tisyn

colp

ites

gig

an

teu

sP

eri

retis

ynco

lpite

sm

ag

no

sag

en

atu

sP

oly

po

dia

ceo

isp

ori

tes

sp.

Re

titri

colp

ites

bre

vico

lpa

tus

Ru

go

po

llen

ites

spS

cab

rast

ep

ha

no

po

rite

s"d

en

sus"

Cla

vatr

ilete

sm

utis

iiR

etim

on

oco

lpite

sre

tifo

ssu

latu

sD

up

lotr

ipo

rite

sa

ria

ni

Pro

xap

ert

ites

op

erc

ula

tus

Psi

lab

revi

tric

olp

ites

"pe

qu

eñ

us"

An

nu

trip

ori

tes

ive

rse

nii

Ech

iste

ph

an

oco

lpite

s"m

inu

tiech

ina

tus"

Fo

veo

trile

tes

ma

rga

rita

eR

etis

tep

ha

no

po

rite

s"s

ea

mro

gifo

rmis

"S

tria

mo

no

lete

s"g

iga

nte

us"

Ru

go

mo

no

colp

ites

"pe

rfe

ctu

s"E

chitr

ilete

s"p

eq

ue

ñu

s"R

etit

rico

lpo

rite

s"i

rre

gu

lari

s"V

err

utr

ilete

s"m

ag

no

ge

mm

atu

s"R

etid

ipo

rite

se

lon

ga

tus

Re

tiste

ph

an

oco

lpite

s"m

inim

us"

Pro

xap

ert

ites

sulc

atu

sC

alli

ala

spo

rite

sd

am

pie

riA

ria

dn

asp

ori

tes

sp.

Ch

om

otr

ilete

sm

ino

rC

lava

spo

rite

ssp

.G

em

ma

mo

no

colp

ites

spR

etin

ap

ert

uri

tes

sp.

Sp

iniz

on

oco

lpite

s"g

em

ma

tus"

Lo

ng

ap

ert

ites

sp.

Cic

atr

ico

sisp

ori

tes

ven

ust

us

Ho

rnie

llalu

na

ren

sis

Ma

gn

ore

titri

lete

s"m

ag

no

viru

ele

nsi

s"S

tria

mo

no

lete

ssp

.

4 2 3 1 20 1 4 2 1 1 1 1 1 5 1 1 183 1 1 3 3 3 1 2 1 1

6 24 6 2 1 3 1 240 1 1 4 4 3 2 4 3 1 4 1 1 1 1 1 1 2 1 2

2 4 57 3 4 2 1 115 4 1 8 2 2 1 1 1 3 1 3 1 1

2 3 2 2 44 1 1 4 3 1 225 1 4 3 2 1 1 2 4 3 1 1 1 2 1 1 1

7 3 3 1 27 2 4 1 1 1 135 3 2 1 3 1 1 1 1 2 2 1 2 1 1 1 1 1 1 1 1 2 1 1

5 3 3 10 2 2 1 4 101 1 1 2 1 1 1 3 1 1 1 1 1 2 1

11 32 1 9 1 175 5 1 4 2 2 1 2 2 1 1 1 1 1 1 1 1 1

3 40 1 1 117 2 1 1 2 2 5 1 1 1

8 1 1 18 1 2 1 2 113 4 1 3 5 1 1 1 3 2 1 1 2 1

7 1 9 1 50 10 5 3 1 139 8 9 14 6 4 9 9 1 1 4 1 8 3 6 1 2 2 2 1 1 2 1 2 1 1 1 1

1 1 67 1 1 2 92 1 13 17 1 1

4 2 6 4 10 5 1 45 1 11 2 1 1 1 1 2 1 1

8 2 1 1 12 2 2 2 4 1 61 1 1 5 1 4 2 1 1 1 1 1 1 2 2 2 1 1

1 1 3 12 1 1 2 2 1 1 332 5 3 4 2 1 1 1 1 2 2 1 2 2 2 9 1 1 1 1 1 2 1 4

1 21 2 1 1 224 4 7 6 4 1 1 1 1 3 2

1 1 1 21 2 7 2 2 114 3 5 3 1 2 3 6 25 1 1 7 1 1 1 1 1 3 1 2 2 4 1

2 25 1 8 5 98 3 5 6 3 5 1 1 3 1 3 1 2 1

9 2 14 1 5 3 1 144 1 3 2 1 4 1 6 3 1 3 1 1 2 1 1 1 2 2 1 1 4 1 1 2 1 2 1 1 1 1 1 1 1

2 15 1 1 1 1 1 2

1 6 7 2 2 1 1 1 1 6 2 1 1 1

8 2 11 7 1 4 2 1 1 104 2 7 1 4 2 1 2 2 4 2 3 1 1 2 1 1 1 1

5 1 3 1 1 17 3 2 1 1 1 5 1 1

8 1 12 1 3 1 1 1 1 10 2 4 2 1 7 1 3 2 5 2 1 2 1 1 1 1 2 1 1 1 1

Spores And PollenAbsolute abundance (40mm=250 counts)

Sp

inife

rite

ssp

.A

nd

alu

sie

llap

oly

mo

rph

aC

ero

din

ium

sp.

Din

ocy

stu

nd

iffL

ing

ulo

din

ium

sp.

Se

ne

ga

liniu

msp

.O

pe

rcu

lod

iniu

msp

.C

ord

osp

ha

eri

diu

msp

.H

ystr

ich

oko

lpo

ma

sp.

Exo

cho

sph

ae

rid

ium

spP

ala

eo

cyst

od

iniu

msp

Flo

ren

tinia

aff

ma

nte

llii

1

131 1 3 1 4

1 1

2 1

1 1

1

1

1

1 2 1

1 1 1

5 4 1

2 1

3 1

1 4

Dinoflagellate Cysts*2

Le

iosp

ha

eri

dia

sp.

Pte

rosp

erm

op

sis

sp.

Po

lykr

iko

s?sp

.

4

3

1

1

AC*2

Inse

rta

ese

dis

1

MM

*2

Alg

ae

typ

eP

ed

iast

rum

sp.

1 1

1

2

2

7

1

5

2

2

4

10

1

1

ALBO

*2

Fo

ram

test

linin

g

1

2

2

4

1

6

1

2

2

2

1

1

1

3

1

FT

*2

Fu

ng

i.

Myc

roth

iria

cite

ssp

.D

ipo

rop

olli

sa

ssa

mic

a

39

77

18

92

66

41

21

3825

68

23

8

18 1

9

7

11

33

23 1

3

3

86

10 1

29

FungiAbsolute abundance (40mm=250 counts)

Tota

lco

un

ting

Tota

lMa

rin

e

248

325 2

219 2

320 2

246 27

150 1

259

190 12

181 1

333 5

210 7

102 1

128 1

408 1

291 7

239 3

175 1

248 11

28 4

37 3

181 2

48 4

87 6

Total

Tota

lco

un

t:S

po

res

An

dP

olle

n

250

248

321

217

317

217

149

257

178173

327

198

99

124

407

280

226

174

235

24

33

179

43

81

Spores And Pollen

Samples

Sam

ple

sin

Dis

ciplin

e(s

):

Paly

9.10

20.00

28.00

38.30

48.00

56.00

68.00

84.0087.70

99.70

108.00

121.70

128.00

140.00

148.00

161.10

172.00

184.00

196.00

208.10

220.00

232.00

244.00

Depth

50m

100m

150m

200m

250m

APPENDIX A. Quantitative distribution of palynomorphs in Core PPI-3 (Middle Umir Formation) expressed in absolute abundances

Interval : 0m - 264m

Scale : 1:2500

Text Keys

*1 Longapertites proxapertitoides var proxapertitoides

*2 Absolute abundance (40mm=250 counts)

62

6563

APPENDIX B QUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN CORE PPM-5 (MIDDLE UMIR


Depth

50m

100m

150m

200m

250m

300m

Samples

Sam

ple

sin

Dis

ciplin

e(s

):

Paly

32.00

44.10

56.00

68.80

78.45

88.00

100.30

112.00

125.50

137.00

160.00

172.05

184.15

216.00

230.50

243.00

253.00

267.60

280.00


Ara

uca

ria

cite

sa

ust

ralis

Bu

ttin

iaa

nd

ree

viC

alli

ala

spo

rite

sd

am

pie

riE

chim

on

oco

lpite

sp

roto

fra

nci

sco

i

Ech

itrile

tes

aca

nth

otr

ileto

ide

sE

chitr

ilete

s"p

roto

mu

elle

ri"E

chitr

ipo

rite

str

ian

gu

lifo

rmis

Ga

bo

nis

po

ris

vig

oro

uxi

iG

em

ma

trile

tes

sp.

Lo

ng

ap

ert

ites

pro

xap

ert

itoid

es

var.

irre

gu

lari

sM

ue

rrig

eri

spo

ris

"ard

ilen

sis"

Psi

latr

ilete

sg

rou

p

Re

tibre

vitr

ico

lpo

rite

s"r

etic

ula

tus"

Sca

bra

trile

tes

gra

nu

lari

sS

pin

izo

no

colp

ites

ba

cula

tus

Sp

iniz

on

oco

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s"b

revi

ba

cula

tus"

Ulm

oid

eip

ites

kre

mp

iiA

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pite

ssp

.C

rusa

fon

tite

sg

ran

dio

sus

Dip

oro

con

iacf

.D

ipo

roco

nia

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asz

en

tgyo

erg

yi

Mo

no

colp

op

olle

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s"m

icro

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s"P

eri

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iga

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us

Pro

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ites

hu

mb

ert

oid

es

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ico

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sh

am

me

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iniz

on

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lava

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eR

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no

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ites

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nd

ufo

uri

oid

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ites

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ph

ina

eA

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ers

en

iiB

acu

mo

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om

on

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usa

eE

ph

ed

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on

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po

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ites

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Psi

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ico

lpo

rite

s"s

cab

ratu

s"S

pin

izo

no

colp

ites

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iniv

err

uco

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iatr

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rite

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tra

dite

su

mir

en

sis

Ve

rru

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tes

"ma

gn

ovi

rue

loid

es"

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plo

trip

ori

tes

ari

an

iH

am

ula

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ori

sca

pe

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eri

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sm

ag

no

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en

atu

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on

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cab

rast

ep

ha

no

colp

ori

tes

gu

ad

ue

nsi

sA

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pite

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gio

Cla

vasp

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tes

mu

tisii

Re

tidip

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err

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rue

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imo

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ites

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chye

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atu

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ilete

sin

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ole

nsi

sG

em

ma

mo

no

colp

ites

dis

pe

rsu

sM

on

oco

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sg

ran

dis

pin

ige

rP

rote

aci

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sd

eh

aa

ni

Re

timo

no

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ites

cla

ris

Re

titri

colp

ites

sp.

Ru

gu

latis

po

ris

spS

tep

ha

no

colp

ites

cost

atu

sZ

livis

po

ris

bla

ne

nsi

sE

chitr

ico

lpite

s"i

nm

en

sus"

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bra

ste

ph

an

op

ori

tes

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nsu

s"C

ing

ula

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rru

catu

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eri

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acu

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rite

se

xin

am

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ynd

em

ico

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sty

pic

us

Aq

uila

po

llen

ites

ma

gn

us

Ba

cula

mo

no

colp

ites

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cula

inte

rru

ptu

s"H

orn

iella

lun

are

nsi

sL

on

ga

pe

rtite

sp

roxa

pe

rtito

ide

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r.re

ticu

loid

es

Re

tipo

llen

ites

"afr

op

olle

nsi

s"P

sila

dip

ori

tes

"op

erc

ula

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Psi

latr

ico

lpite

ssp

.R

etid

ipo

rite

sm

ag

da

len

en

sis

Tetr

aco

lpo

rop

olle

nite

s"p

roto

tra

nsv

ers

alis

"C

ho

mo

trile

tes

min

or

Psi

lab

revi

tric

olp

ites

ma

rgin

atu

sC

olo

mb

ipo

llis

tro

pic

alis

Mo

no

colp

op

olle

nite

s"r

etic

ula

tus"

Psi

latr

ipo

rite

ssp

.R

etid

ipo

rite

se

lon

ga

tus

Ba

cutr

ilete

s"p

roxi

ma

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Fo

veo

trile

tes

ma

rga

rita

eC

yca

do

pite

ssp

.E

chis

tep

ha

no

colp

ites

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utie

chin

atu

s"E

chitr

ilete

s"d

ista

verr

uca

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Pro

xap

ert

ites

"he

tero

gra

nd

isp

inig

er"

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xap

ert

ites

psi

latu

sP

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bre

vitr

ico

lpo

rite

sa

nn

ula

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colp

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err

utr

ico

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on

ga

pe

rtite

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ove

ola

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lam

on

oco

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so

pe

rcu

latu

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ria

dn

ae

spo

rite

ssp

.P

sila

dip

ori

tes

min

imu

s

1 1 1 17 1 3 1 1 1 1 2 38 1 3 1 1 1

1 4 3 4 25 1 1 1 1 1 1 1 2 1

1 2 3 1 3

4 6 1 1 166 3 2 2 1 1 1

1 3 4 9 1

4 10 1 2 37 3 1 2 1 1 1 1 2 1 1 1 1 1 1 1 2 1

13 2 1 96 1 3 2 1 1 1 3 1 1 1 1 1 3 1

3 1 16 300 2 2 3 1 2 2 1 1 1 1 1 1 1

4 3 27 1 5 230 5 3 1 3 2 2 1 1 1 1 1 1 1 2 3 1 1 1 1 1 2 2 1 1

1 1 30 1 2 3 120 3 2 2 1 1 1 1 2 3 1 1 1 1

43 3 1 174 2 1 3 2 1 1 1 3 1 2 1 2 4

4 6 18 3 2 6 52 5 7 3 1 1 1 5 2 1 1 1 1 1 1 1 1 2 1 1 1 1 1 1 1

7 33 11 1 1 221 20 6 1 5 1 3 1 1 1 4 2 11 1 1 1 1 1 1 1

10 3 37 3 3 134 7 3 3 6 1 2 1 3 1 1 1 5 1 2 1 1 1 1 1

20 45 4 172 1 22 4 3 3 17 1 1 4 4 1 1 6 2 4 1 2 1 1 1 1

3 11 1 221 3 4 50 3 5 4 1 2 1 1 1 1 1 3

22 2 43 1 1 1 12 1 171 2 13 2 2 3 3 7 1 3 1 1 2 1 2 7 6 3 3 1 2 1 2 1 1 1 1

24 2 112 2 4 1 1 98 11 3 3 29 2 1 1 1 1 1 1 1 2 6 1 1 1 1 1

8 2 113 4 158 6 3 1 1 14 4 3 1 1 1 1 1 1 4 2 1 1


An

da

lusi

ella

-P

ala

eo

cyst

od

iniu

mco

mp

lex

Din

ocy

stu

nd

iffF

ibro

cyst

asp

.S

en

eg

alin

ium

sp.

Sp

inife

rite

ssp

.A

nd

alu

sie

llasp

.E

xoch

osp

ha

eri

diu

msp

Ce

rod

iniu

msp

eci

osu

mS

en

eg

alin

ium

mic

rosp

ino

sum

Ce

rod

iniu

md

ieb

elii

Gla

ph

yro

cyst

asp

An

da

lusi

ella

ga

bo

ne

nsi

sD

ino

gym

niu

msp

.D

ino

gym

niu

ma

cum

ina

tum

3 2 1 5 1

2 2

1 1

1 1 1

1

4

2 2 5 2 1 1 1

2 1 1

1

1 1 1 1

1 1 6

1 1 1

1 1


Le

iosp

ha

eri

dia

sp.

1

AC

*1

Pe

dia

stru

msp

.A

lga

ety

pe

1

1

1

3

1

1

ALBO

*1

Fo

ram

test

linin

g

2

1

1

1

5

4

12

1

FT

*1

Cru

sta

cea

ne

gg

s

1

MM

*1

Fu

ng

i.

18

20

6

60

11

44

49

51

24

41

38

19

32

24

61

35

25

45

32


Tota

lco

un

ting

Tota

lMa

rin

e

89 14

51 4

12 2

187

23 4

78 1

137 4

340

323 14

182 4

250 2

139 6

336

241 9

327 5

316

332 7

325 12

335 3

Total

Tota

lco

un

t:S

po

res

An

dP

olle

n

300

75

47

10

188

18

76

133

339

309

178

245

133

337

232

322

316

326

312

331

Spores And Pollen

Samples

Sam

ple

sin

Dis

ciplin

e(s

):

Paly

32.00

44.10

56.00

68.80

78.45

88.00

100.30

112.00

125.50

137.00

160.00

172.05

184.15

216.00

230.50

243.00

253.00

267.60

280.00

Depth

50m

100m

150m

200m

250m

300m


Scale : 1:2500

Text Keys*1Absolute abundance (40mm=300 counts)

APPENDIX B. Quantitative distribution of palynomorphs in Core PPM-5 (Middle Umir Formation) expressed in absolute abundances

64

65

APPENDIX CQUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN CORE PPM-2 (MIDDLE -

UPPER UMIR FORMATION) EXPRESSED IN ABSOLUTE ABUNDANCES

Depth

50m

100m

150m

200m

250m

Samples

Sam

ple

sin

Dis

ciplin

e(s

):

Paly

30.00

41.00

49.80

63.00

74.70

87.00

97.40

109.90

121.50

134.00

146.30

158.00

170.40

182.00

194.40

206.30212.40

224.10

236.75

249.05

262.20

273.00


Ch

om

otr

ilete

sm

ino

rD

ipo

roco

nia

cfD

ipo

roco

nia

iszk

asz

en

tgyo

erg

yiE

chim

on

oco

lpite

sp

ach

yexi

na

tus

Ech

imo

no

colp

ites

pro

tofr

an

cisc

oi

Ech

itrile

tes

"aca

nth

otr

ileto

ide

s"E

chitr

ipo

rite

ssu

esc

ae

Ep

he

dri

pite

ssp

.F

ove

otr

ilete

sm

arg

ari

tae

Mo

no

colp

ites

gra

nd

isp

inig

er

Mo

no

colp

op

olle

nite

ssp

.M

ue

rrig

eri

spo

ris

"ard

ilen

sis"

Po

lyp

od

iace

ois

po

rite

ssp

.P

rote

aci

dite

sd

eh

aa

ni

Pro

xap

ert

ites

hu

mb

ert

oid

es

Pro

xap

ert

ites

op

erc

ula

tus

Pro

xap

ert

ites

psi

latu

sP

roxa

pe

rtite

ssu

lca

tus

Psi

latr

ico

lpite

sh

am

me

nii

Psi

latr

ilete

sg

rou

p

Re

titri

colp

ites

jose

ph

ina

eS

cab

ratr

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sg

ran

ula

ris

Sp

iniz

on

oco

lpite

s"b

revi

ba

cula

tus"

Ste

ph

an

oco

lpite

sco

sta

tus

Ve

rru

trile

tes

viru

elo

ide

sZ

on

otr

ico

lpite

sva

ria

bili

sA

nn

utr

ipo

rite

siv

ers

en

iiA

reci

pite

sre

gio

Co

lom

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olli

str

op

ica

lisE

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rite

str

ian

gu

lifo

rmis

Ga

bo

nis

po

ris

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oro

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ula

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ori

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pe

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eri

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sm

ag

no

sag

en

atu

sP

oly

po

diis

po

rite

ssp

.P

roxa

pe

rtite

s"r

etic

ulo

dim

inu

tus"

Pro

xap

ert

ites

verr

uca

tus

Psi

lam

on

oco

lpite

so

pe

rcu

latu

sR

etim

on

oco

lpite

ssp

.S

pin

izo

no

colp

ites

ba

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Syn

de

mic

olp

ites

typ

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sTe

tra

dite

su

mir

en

sis

Ve

rru

cato

spo

rite

ssp

.Z

livis

po

ris

bla

ne

nsi

sA

rau

cari

aci

tes

au

stra

lisB

uttin

iaa

nd

ree

viE

chitr

ilete

s"p

roto

mu

lleri"

Re

tipo

llen

ites

"afr

op

olle

nsi

s"A

qu

ilap

olle

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Ge

mm

am

on

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isp

ers

us

Lo

ng

ap

ert

ites

pro

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es

va

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es

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ntit

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gra

nd

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sS

pin

izo

no

colp

ites

"cla

vatu

s"K

uyl

isp

ori

tes

wa

terb

olk

iiR

etit

rico

lpite

sb

revi

colp

atu

sR

etit

rico

lpo

rite

ssp

.V

err

utr

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sm

ag

no

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elo

ide

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ori

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Re

timo

no

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ites

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oss

ula

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Syn

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ori

tes

lisa

ma

eN

eo

rais

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kia

"co

nst

rict

us"

Psi

lab

revi

tric

olp

ori

tes

an

nu

latu

sD

up

lotr

ipo

rite

sa

ria

ni

Psi

lab

revi

tric

olp

ori

tes

sim

plif

orm

isR

etin

ap

ert

uri

tes

"dim

inu

tus"

Ba

cum

orp

ho

mo

no

colp

ites

tau

sae

Ulm

oid

eip

ites

kre

mp

iiC

lava

spo

rite

sm

utis

ii

1 1 1 98 1 1 1 3 1 1 2 1 5 1 2 2 2 1 157 3 4 2 3 1 2

5 17 2 1 2 1 1 1 2 54 2 3 182 3 1 3 3 1 4 4 11 5 1 1 1 2 10 1 1 5 2 1 1 1

5 5 1 10 2 1 1 1 1 1

2 1 1 2

4 1 1 1 1 23 1 1 1 1 2 1

8 3 44 2 1 1 1 1 1 1

73 1 51 93 5 3 1 1 2 1 1

1 222 1 3 95 3 2 1 2 2 1 2 1

1 14 1 1 1 1 2 239 1 1 3 1

1 1 21 1 3 3 1 16 240 3 1 3 1 2 1 4 1 2 12 4 1 1 2 1

1 51 2 3 3 2 1 1 19 63 1 25 1 2 3 1 1 1 1 1 13 2 4 5 1 1 1 2

4 13 1 1 1 1 1 1 4 298 1 10 2 1 1 1 1 1 2 1 1 2 1

1 2 44 5 4 5 93 1 79 4 1 3 2 1 1 4 1 1 1 1 1

1 33 1 6 2 1 2 28 73 22 1 1 7 1 7 1 1 1 1 2

1 55 2 1 1 1 9 202 7 1 4 1 1 11 2 1 1 1 1 1 1 1 1

1 168 1 9 1 21 77 4 1 2 2 1 2 14 1 1 1 1 3

8 6 1 1 1 1 1 2 1 3 1

5 48 1 2 2 1 2 16 2 110 2 45 1 3 3 8 3 1 2 5 1 1 11 2 1 1 2 4 1

1 2 67 3 2 10 2 5 170 3 14 1 1 1 1 3 1 6 2 1 7 2 3 1 1 1 1

4 18 11 2 1 1 127 1 18 2 1 1 13 50 4 2 1 1 6 2

1 40 2 3 282 1 4 1 1 1 4 1 1

1 33 1 1 259 15 2 1 2 10 1 1


An

da

lusi

ella

-P

ala

eo

cyst

od

iniu

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mp

lex

An

da

lusi

ella

ga

bo

ne

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nd

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sie

llasp

.C

ero

din

ium

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ocy

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osp

ha

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Pa

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ium

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en

eg

alin

ium

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Sp

inife

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ibro

cyst

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.M

an

um

iella

see

lan

dic

aA

cho

mo

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.C

ero

din

ium

spe

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sum

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om

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ulif

era

Hys

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ium

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Ph

elo

din

ium

spL

ing

ulo

din

ium

sp.

An

da

lusi

ella

rho

mb

oid

es

Are

olig

era

sen

on

en

sis

Co

rdo

sph

ae

rid

ium

sp.

Din

og

ymn

ium

.F

lore

ntin

iam

an

telli

iH

ystr

ich

oko

lpo

ma

sp.

3 3 5 1 1 1 1 6 1 2

1

2 2

3 1 1

1 2

5 1 8 1 1 1

5

3 11 21 5 1 1 1

1

4 2 7 1 1

4 6 4 2

7 1 3 3

1 1 1 1 1 1 3 1

1 2 1

1

3 4 5


Le

iosp

ha

eri

dia

sp.

2

3

9

AC

*1

Pe

dia

stru

msp

.(C

om

pa

cto

)

3

1

1

5

3

10

1

1

*2

*1

Fo

ram

linn

ing

1

1

5

1

2

FT

*1

Fu

ng

i.

2

1

3

4

11

2

14

19

23

15

17

12

4

17

5

22

10

FU


Tota

lco

un

ting

Tota

lMa

rin

e

325 25

335

29 1

10 4

43 5

67 4

248 17

336

266

331 5

254 48

352 2

264 17

208 16

318 14

31128 2

298 13

316 4

275 9

343 1

334 12

Total

Tota

lco

un

t:S

po

res

An

dP

olle

n

300

297

335

28

6

38

63

232

336

266

326

212

350

255

192

307

31126

286

312

266

342

327

Spores And Pollen

Samples

Sam

ple

sin

Dis

ciplin

e(s

):

Paly

30.00

41.00

49.80

63.00

74.70

87.00

97.40

109.90

121.50

134.00

146.30

158.00

170.40

182.00

194.40

206.30212.40

224.10

236.75

249.05

262.20

273.00

Depth

50m

100m

150m

200m

250m


Scale : 1:2500

Text Keys


*2 ALBO

APPENDIX C. Quantitative distribution of palynomorphs in Core PPM-2 (Middle - Upper Umir Formation) expressed in absolute abundances

66

67

APPENDIX DQUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN CORE PPM-1 (UPPER UMIR


69

Depth

50m

100m

150m

Samples

Sam

ple

sin

Dis

ciplin

e(s

):

Paly

23.5426.00

32.70

42.00

51.93

60.00

72.25

85.80

92.05

104.50

115.25

124.00

133.20

143.00

152.00

160.00


Are

cip

ites

reg

ioC

alli

ala

spo

rite

sd

am

pie

riC

lava

spo

rite

sm

utis

iiC

olo

mb

ipo

llis

tro

pic

alis

Cru

safo

ntit

es

gra

nd

iosu

sE

chim

on

oco

lpite

sp

ach

yexi

na

tus

Ech

imo

no

colp

ites

pro

tofr

an

cisc

oi

Ech

itrile

tes

pro

tom

ulle

riE

chitr

ipo

rite

ssu

esc

ae

Ep

he

dri

pite

sg

iga

nte

us

Fo

veo

trile

tes

ma

rga

rita

eG

em

ma

mo

no

colp

ites

dis

pe

rsu

s*1 M

on

oco

lpo

po

llen

ites

sp.

Pro

xap

ert

ites

hu

mb

ert

oid

es

Pro

xap

ert

ites

op

erc

ula

tus

Pro

xap

ert

ites

verr

uca

tus

Psi

latr

ico

lpite

sh

am

me

nii

Psi

latr

ilete

sg

rou

p

Re

tipo

llen

ites

afr

op

olle

nsi

sS

cab

ratr

ilete

sg

ran

ula

ris

Sp

iniz

on

oco

lpite

sb

acu

latu

sS

tep

ha

no

colp

ites

cost

atu

sV

err

utr

ilete

svi

rue

loid

es

Ga

bo

nis

po

ris

vig

oro

uxi

iR

etit

rico

lpite

sjo

sep

hin

ae

Bu

ttin

iaa

nd

ree

viE

chitr

ilete

sa

kan

tho

trile

toid

es

Mu

err

ige

risp

ori

s"a

rdile

nsi

s"P

rote

aci

dite

sd

eh

aa

ni

Psi

lab

revi

tric

olp

ites

an

nu

latu

sP

sila

bre

vitr

ico

lpo

rite

s"d

imin

utu

s"U

lmo

ide

ipite

skr

em

pii

Dic

olp

op

olli

ssp

.M

on

oco

lpite

sg

ran

dis

pin

ige

rP

roxa

pe

rtite

sp

sila

tus

Pro

xap

ert

ites

sulc

atu

sR

etib

revi

tric

olp

ori

tes

sp.

Re

titri

colp

ori

tes

sp.

Syn

de

mic

olp

ites

typ

icu

sTe

tra

dite

su

mir

en

sis

Zo

no

tric

olp

ites

vari

ab

ilis

Cyc

ad

op

ites

sp.

Du

plo

trip

ori

tes

ari

an

iH

orn

iella

lun

are

nsi

sL

on

ga

pe

rtite

ssp

.S

pin

izo

no

colp

ites

ech

ina

tus

Ve

rru

mo

no

colp

ites

sp.

Zliv

isp

ori

sb

lan

en

sis

Cla

vatr

ico

lpite

s"d

imin

utu

s"D

ipo

roco

nia

cfD

ipo

roco

nia

iszk

asz

en

tgyo

erg

yiH

am

ula

tisp

ori

sca

pe

ratu

sL

on

ga

pe

rtite

sva

ne

en

de

nb

urg

iP

eri

retis

ynco

lpite

sg

iga

nte

us

Pe

rire

tisyn

colp

ites

ma

gn

osa

ge

na

tus

Re

timo

no

colp

ites

sp.

Syn

colp

ori

tes

lisa

ma

eS

ynco

lpo

rite

sm

arg

ina

tus

Ch

om

otr

ilete

sm

ino

rL

ae

vig

ato

spo

rite

sg

ran

ula

ris

An

nu

trip

ori

tes

ive

rse

nii

Aq

uila

po

llen

ites

spP

sila

bre

vitr

ico

lpo

rite

ssi

mp

lifo

rmis

Ve

rru

trile

tes

ma

gn

ovi

rue

loid

es

Po

lya

dite

ssp

.P

oly

po

diis

po

rite

ssp

.P

sila

mo

no

colp

ites

op

erc

ula

tus

Ep

he

dri

pite

ssp

p.

Sp

iniz

on

oco

lpite

s"c

lava

tus"

Sp

iniz

on

oco

lpite

sin

tra

rug

ula

tus

Re

timo

no

colp

ites

retif

oss

ula

tus

Re

tisyn

colp

ori

tes

"min

imu

s"R

etit

rico

lpite

sb

revi

colp

atu

sB

acu

mo

rph

om

on

oco

lpite

sta

usa

eE

chitr

ilete

ssp

.S

cab

rast

ep

ha

no

po

rite

s"d

en

sus"

Sp

iniz

on

oco

lpite

s"b

revi

ba

cula

tus"

Ara

uca

ria

cite

sa

ust

ralis

Lo

ng

ap

ert

ites

pro

xap

ert

itoid

es

var

retic

ulo

ide

sF

ove

om

on

oco

lpite

s"h

ete

rofo

veo

latu

s"P

od

oca

rpid

ites

sp

4 1 1 3 6 2 89 2 1 1 16 1 1 1 5 5 2 2 126 3 131 1 1

140 3 5 1 1 1 229 1 1 2 4

2 1 21 1 18 4 4 239 1 1 4 1 1 2 1 1 1 7

6 7 30 2 3 5 1 8 79 6 2 3 1 5 1 1 1 1 1 2 2 1 1 2 2 1

5 9 17 2 3 4 2014 4 55 5 1 3 4 2 1 1 1 1 1 1 1 1 2

9 2 35 2 4 1 1 4 7 4 111 2 9 6 1 1 4 1 1 2 1 1 1 1 1 1 1 1 1 1 1

1 1 3 1 1 1 8 1

4 36 5 2 1 1 3 5 37 131 1 1 1 3 3 1 1

1 1 1 15 1 13 2 2 1 3 1 295 1 4 1 1 1 2 1 1 1 1 1 1 1 1

3 2 33 1 2 5 8 169 2 3 2 2 1 4 3 1 2 1 1 1 1 1

4 65 2 2 2 1 1 2 123 4 1 1 1 1 1 1 1 1 2 1 1 1

2 2 1 12 1 1 1 1 2 305 1 1 1 1 1 2 1 2 1 1

6 20 5 1 3 1 1 1 95 6 1 1 1 1 3 2 6 1 1 1 2 1 4

3 2 35 2 1 1 2 1 1 8 133 18 3 1 1 2 2 1 1 1 1 1 1 1 1 1 3

9 1 58 2 2 1 1 2 15 100 1 4 6 1 2 1 5 1 1 1 2 1 1 1 1 1 1 1 1 2 10 1

1 16 2 2 1 6 15 1 3 2 2 3 1 1 2 1 5 5 1 1


An

da

lusi

ella

sp.

Sp

inife

rite

ssp

.A

cho

mo

sph

ae

rasp

.

Aly

sog

ymn

ium

eu

cla

en

seA

nd

alu

sie

lla-

Pa

lae

ocy

sto

din

ium

com

ple

xA

nd

alu

sie

llag

ab

on

en

sis

An

da

lusi

ella

ma

uth

ei

An

da

lusi

ella

po

lym

orp

ha

An

da

lusi

ella

rho

mb

oid

es

Ce

rod

iniu

msp

.F

ibro

cyst

asp

.H

ystr

ich

oko

lpo

ma

bu

lbo

sum

Ma

nu

mie

llase

ela

nd

ica

Pa

lae

ocy

sto

din

ium

au

stra

linu

mA

cho

mo

sph

ae

rara

mu

life

raC

ord

osp

ha

eri

diu

msp

.D

ino

cyst

un

diff

Hys

tric

ho

sph

ae

rid

ium

spL

ing

ulo

din

ium

sp.

Olig

osp

ha

eri

diu

msp

.P

ala

eo

cyst

od

iniu

msp

Are

olig

era

sen

on

en

sis

Hys

tric

ho

din

ium

sp.

Flo

ren

tinia

ma

nte

llii

Hys

tric

ho

kolp

om

asp

.P

ala

eo

cyst

od

iniu

mg

olz

ow

en

se

2 2

31 4 3 1 7 2 4 11 1 2 8 1 2 1

4 6 39 3 7 3 2 1 16 2 3 4 1

17 5 23 1 1 1 1 10 2 1 1 2

1

1214 4 7 3 1

8 2

2 2 3

2 1 1 1

3 1 6 2 1 1

4 9 3 1 3 1 1 5 2 1

1 6 1


Le

iosp

ha

eri

dia

sp.

1

1

2

AC

*2

Pe

dia

stru

msp

.(C

om

pa

cto

)A

lga

ety

pe

1

3

1

ALBO

*2

Fo

ram

linn

ing

1

1

1

1

1

1

1

3

FT

*2

Fu

ng

i.

Myc

roth

iria

cite

ssp

.

146

14

24

38

45

31

28

30

51

53 3

32

43


Tota

lco

un

ting

Tota

lMa

rin

e

295 6

388

310

183 79

180 94

228 66

17 1

136 42

357

256 10

221 7

340 5

165 1

235 15

243 31

76 11

Total

Tota

lco

un

t:S

po

res

An

dP

olle

n

250

288388

310

174

158

218

17

119

354

248

219

340

164

228

237

71

Spores And Pollen

Samples

Sam

ple

sin

Dis

ciplin

e(s

):

Paly

23.5426.00

32.70

42.00

51.93

60.00

72.25

85.80

92.05

104.50

115.25

124.00

133.20

143.00

152.00

160.00

Depth

50m

100m

150m


Scale : 1:2000

Text Keys

*1 Longapertites proxapertitoides var proxapertitoides


APPENDIX D. Quantitative distribution of palynomorphs in Core PPM-1 (Upper Umir Formation) expressed in absolute abundances

68

69

APPENDIX ERANGE CHART OF PALYNOMORPHS IN THE UMIR FORMATION, SAN LUIS AREA,

MIDDLE MAGDALENA VALLE BASIN (MMVB)

Depth

50m

100m

150m

200m

250m

300m

350m

400m

450m

500m

550m

600m

650m

700m

750m

800m

850m

Samples

Sam

ple

sin

Dis

cip

line(s

):

Paly

2.46 PPM-1 26

9.16 PPM-1 32.7

18.46 PPM-1 42

28.39 PPM-1 51.93

36.46 PPM-1 60

48.71 PPM-1 72.25

62.26 PPM-1 85.868.51 PPM-1 92.0574.46 PPM-1 3080.96 PPM-1 104.585.46 PPM-2 4191.71 PPM-1 115.2594.26 PPM-2 49.8100.46 PPM-1 124107.46 PPM-2 63109.66 PPM-1 133.2119.16 PPM-2 74.7119.46 PPM-1 143128.46 PPM-1 152131.46 PPM-2 87136.46 PPM-1 160141.86 PPM-2 97.4

154.36 PPM-2 109.9

165.96 PPM-2 121.5

178.46 PPM-2 134

190.76 PPM-2 146.3

202.46 PPM-2 158

214.86 PPM-2 170.4

226.46 PPM-2 182

238.86 PPM-2 194.4

250.76 PPM-2 206.3256.86 PPM-2 212.4

268.56 PPM-2 224.1

281.21 PPM-2 236.75

293.51 PPM-2 249.05

306.66 PPM-2 262.2

317.46 PPM-2 273

324.46 PPM-5 32

336.56 PPM-5 44.1

348.46 PPM-5 56

361.26 PPM-5 68.8

370.91 PPM-5 78.45

380.46 PPM-5 88

392.76 PPM-5 100.3

404.46 PPM-5 112

417.96 PPM-5 125.5

429.46 PPM-5 137

452.46 PPM-5 160

464.51 PPM-5 172.05

476.61 PPM-5 184.15

508.46 PPM-5 216

522.96 PPM-5 230.5

535.46 PPM-5 243

545.46 PPM-5 253

560.06 PPM-5 267.6

572.46 PPM-5 280

632.46 PPI-3 9.1

643.36 PPI-3 20

651.36 PPI-3 28

661.66 PPI-3 38.3

671.36 PPI-3 48

679.36 PPI-3 56

691.36 PPI-3 68

707.36 PPI-3 84711.06 PPI-3 87.7

723.06 PPI-3 99.7

731.36 PPI-3 108

745.06 PPI-3 121.7

751.36 PPI-3 128

763.36 PPI-3 140

771.36 PPI-3 148

784.46 PPI-3 161.1

795.36 PPI-3 172

807.36 PPI-3 184

819.36 PPI-3 196

831.46 PPI-3 208.1

843.36 PPI-3 220

855.36 PPI-3 232

867.36 PPI-3 244

Stratigraphic Range

Ech

imo

no

co

lpite

sp

roto

fra

ncis

co

iE

ch

itri

lete

s"p

roto

mu

elle

ri"F

ove

otr

ilete

sm

arg

ari

tae

Ga

bo

nis

po

ris

vig

oro

uxii

Ge

mm

am

on

oco

lpite

sd

isp

ers

us

Pro

xa

pe

rtite

so

pe

rcu

latu

sP

roxa

pe

rtite

sve

rru

ca

tus

Psila

trile

tes

gro

up

Re

titr

ico

lpite

sjo

se

ph

ieS

tep

ha

no

co

lpite

sco

sta

tus

Ve

rru

trile

tes

vir

ue

loid

es

Are

cip

ite

sre

gio

Bu

ttin

iaa

nd

ree

vi

Ca

llia

lasp

ori

tes

da

mp

ieri

Cla

va

sp

ori

tes

mu

tisii

Ech

itri

lete

s"a

ca

nth

otr

ileto

ide

s"E

ch

itri

po

rite

ssu

esca

eM

ue

rrig

eri

sp

ori

s"a

rdile

nsis

"P

rote

acid

ite

sd

eh

aa

ni

Psila

bre

vitri

co

lpo

rite

sa

nn

ula

tus

Psila

bre

vitri

co

lpo

rite

s"d

imin

utu

s"R

etip

olle

nite

s"a

fro

po

llen

sis

"S

ca

bra

trile

tes

gra

nu

lari

sU

lmo

ide

ipite

skre

mp

iiC

olo

mb

ipo

llis

tro

pic

alis

Mo

no

co

lpite

sg

ran

dis

pin

ige

rP

roxa

pe

rtite

sh

um

be

rto

ide

sP

roxa

pe

rtite

sp

sila

tus

Pro

xa

pe

rtite

ssu

lca

tus

Psila

tric

olp

ite

sh

am

me

nii

Re

tib

revitri

co

lpo

rite

ssp

.R

etitr

ico

lpo

rite

ssp

.S

pin

izo

no

co

lpite

sb

acu

latu

sS

yn

de

mic

olp

ite

sty

pic

us

Tetr

ad

ite

su

mir

en

sis

Zo

no

tric

olp

ite

sva

ria

bili

sC

yca

do

pite

ssp

.D

up

lotr

ipo

rite

sa

ria

ni

Ho

rnie

llalu

ren

sis

Lo

ng

ap

ert

ite

ssp

.Z

livis

po

ris

bla

ne

nsis

Dip

oro

co

nia

cf.

Dip

oro

co

nia

iszka

sze

ntg

yo

erg

yi

Ha

mu

latisp

ori

sca

pe

ratu

sL

on

ga

pe

rtite

sva

ne

en

de

nb

urg

iP

eri

retisyn

co

lpite

sg

iga

nte

us

Pe

rire

tisyn

co

lpite

sm

ag

no

sa

ge

tus

Re

tim

on

oco

lpite

ssp

.S

yn

co

lpo

rite

slis

am

ae

Ch

om

otr

ilete

sm

ino

rL

ae

vig

ato

sp

ori

tes

gra

nu

latu

sA

nn

utr

ipo

rite

siv

ers

en

iiA

qu

ilap

olle

nite

ssp

Cru

sa

fon

tite

sg

ran

dio

su

s*1 M

on

oco

lpo

po

llen

ite

ssp

.P

sila

bre

vitri

co

lpo

rite

ssim

plif

orm

isV

err

utr

ilete

s"m

ag

no

vir

ue

loid

es"

Ech

imo

no

co

lpite

s"p

ach

ye

xitu

s"E

ph

ed

rip

ite

ssp

p.

Po

lyp

od

iace

ois

po

rite

ssp

.S

pin

izo

no

co

lpite

s"b

revib

acu

latu

s"P

oly

po

diis

po

rite

ssp

.P

sila

mo

no

co

lpite

so

pe

rcu

latu

sE

ch

itri

po

rite

str

ian

gu

lifo

rmis

Sp

iniz

on

oco

lpite

s"c

lava

tus"

Re

tim

on

oco

lpite

sre

tifo

ssu

latu

sR

etitr

ico

lpite

sb

revic

olp

atu

sB

acu

mo

rph

om

on

oco

lpite

sta

usa

eE

ch

itri

lete

ssp

.S

ca

bra

ste

ph

an

op

ori

tes

"de

nsu

s"A

rau

ca

ria

cite

sa

ustr

alis

Lo

ng

ap

ert

ite

sp

roxa

pe

rtito

ide

sva

rre

ticu

loid

es

Psila

tric

olp

ori

tes

sp

.N

eo

rais

tric

kia

"co

nstr

ictu

s"A

recip

ite

ssp

.R

etiste

ph

an

oco

lpite

s"j

an

du

fou

rio

ide

s"S

tria

trip

ori

tes

sp

.S

ca

bra

ste

ph

an

oco

lpo

rite

sg

ua

du

en

sis

Ech

itri

lete

sin

terc

ole

nsis

Re

titr

ico

lpite

ssp

.C

ing

ula

tisp

ori

sve

rru

ca

tus

Aq

uila

po

llen

ite

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acu

lain

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dip

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tes

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Spores And PollenStratigraphic Range

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257247280

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5369

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336

266

110

211

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306

318

71

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65

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41

99

42

243

133

318

223

303

270

322

310

330

229

102

217

316

216

50

257

142172

273

198

90

120

403

280

225

174

232

24

33

88

43

70

Spores And Pollen

Samples

Sam

ple

sin

Dis

cip

line(s

):

Paly

2.46 PPM-1 26

9.16 PPM-1 32.7

18.46 PPM-1 42

28.39 PPM-1 51.93

36.46 PPM-1 60

48.71 PPM-1 72.25


154.36 PPM-2 109.9

165.96 PPM-2 121.5

178.46 PPM-2 134

190.76 PPM-2 146.3

202.46 PPM-2 158

214.86 PPM-2 170.4

226.46 PPM-2 182

238.86 PPM-2 194.4

250.76 PPM-2 206.3256.86 PPM-2 212.4

268.56 PPM-2 224.1

281.21 PPM-2 236.75

293.51 PPM-2 249.05

306.66 PPM-2 262.2

317.46 PPM-2 273

324.46 PPM-5 32

336.56 PPM-5 44.1

348.46 PPM-5 56

361.26 PPM-5 68.8

370.91 PPM-5 78.45

380.46 PPM-5 88

392.76 PPM-5 100.3

404.46 PPM-5 112

417.96 PPM-5 125.5

429.46 PPM-5 137

452.46 PPM-5 160

464.51 PPM-5 172.05

476.61 PPM-5 184.15

508.46 PPM-5 216

522.96 PPM-5 230.5

535.46 PPM-5 243

545.46 PPM-5 253

560.06 PPM-5 267.6

572.46 PPM-5 280

632.46 PPI-3 9.1

643.36 PPI-3 20

651.36 PPI-3 28

661.66 PPI-3 38.3

671.36 PPI-3 48

679.36 PPI-3 56

691.36 PPI-3 68

707.36 PPI-3 84711.06 PPI-3 87.7

723.06 PPI-3 99.7

731.36 PPI-3 108

745.06 PPI-3 121.7

751.36 PPI-3 128

763.36 PPI-3 140

771.36 PPI-3 148

784.46 PPI-3 161.1

795.36 PPI-3 172

807.36 PPI-3 184

819.36 PPI-3 196

831.46 PPI-3 208.1

843.36 PPI-3 220

855.36 PPI-3 232

867.36 PPI-3 244

Scale : 1:2500

Depth

50m

100m

150m

200m

250m

300m

350m

400m

450m

500m

550m

600m

650m

700m

750m

800m

850m

Text Keys*1 Longapertites proxapertitoides var proxapertitoides

*2 Stratigraphic Range

APPENDIX E. Range Chart of palynomorphs in the Umir Formation, San Luis Area, Middle Magdalena Valle Basin (MMVB)

Zo

ne C

Zo

ne B

Zo

ne A

Zo

ne

70

7371

APPENDIX F QUANTITATIVE DISTRIBUTION OF PALYNOMORPHS IN THE UMIR FORMATION,

SAN LUIS AREA, MIDDLE MAGDALENA VALLE BASIN (MMVB)

Depth

50m

100m

150m

200m

250m

300m

350m

400m

450m

500m

550m

600m

650m

700m

750m

800m

850m

Samples

Sam

ple

sin

Dis

cip

line(s

):

Paly

2.46 PPM-1 26

9.16 PPM-1 32.7

18.46 PPM-1 42

28.39 PPM-1 51.93

36.46 PPM-1 60

48.71 PPM-1 72.25


154.36 PPM-2 109.9

165.96 PPM-2 121.5

178.46 PPM-2 134

190.76 PPM-2 146.3

202.46 PPM-2 158

214.86 PPM-2 170.4

226.46 PPM-2 182

238.86 PPM-2 194.4

250.76 PPM-2 206.3256.86 PPM-2 212.4

268.56 PPM-2 224.1

281.21 PPM-2 236.75

293.51 PPM-2 249.05

306.66 PPM-2 262.2

317.46 PPM-2 273

324.46 PPM-5 32

336.56 PPM-5 44.1

348.46 PPM-5 56

361.26 PPM-5 68.8

370.91 PPM-5 78.45

380.46 PPM-5 88

392.76 PPM-5 100.3

404.46 PPM-5 112

417.96 PPM-5 125.5

429.46 PPM-5 137

452.46 PPM-5 160

464.51 PPM-5 172.05

476.61 PPM-5 184.15

508.46 PPM-5 216

522.96 PPM-5 230.5

535.46 PPM-5 243

545.46 PPM-5 253

560.06 PPM-5 267.6

572.46 PPM-5 280

632.46 PPI-3 9.1

643.36 PPI-3 20

651.36 PPI-3 28

661.66 PPI-3 38.3

671.36 PPI-3 48

679.36 PPI-3 56

691.36 PPI-3 68

707.36 PPI-3 84711.06 PPI-3 87.7

723.06 PPI-3 99.7

731.36 PPI-3 108

745.06 PPI-3 121.7

751.36 PPI-3 128

763.36 PPI-3 140

771.36 PPI-3 148

784.46 PPI-3 161.1

795.36 PPI-3 172

807.36 PPI-3 184

819.36 PPI-3 196

831.46 PPI-3 208.1

843.36 PPI-3 220

855.36 PPI-3 232

867.36 PPI-3 244

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14 3 5 2 1 1 1 138 4 1 1

21 1 4 4 136 4 2 1 1 1 1 18 2 1 1 1 1 1 7

3 1 5 1 64 5 3 6 2 1 1 1 6 7 1 3 2 2 8 1 1 2 2 2 1

17 2 4 3 14 55 4 1 5 3 2 5 9 1 2 4 1 1 1 1 1 2

35 2 1 1 1 7 111 4 1 9 4 1 1 2 9 2 4 2 4 6 1 1 1 1 1 1 1 1 1

3 1 1 8 1 1 1 1

36 2 1 1 3 37 1 1 4 5 13 1 3 5 1 3 1 1

15 1 2 3 125 1 1 1 131 2 1 1 1 1 1 1 4 1 1 1 1 2 1 1 1

98 3 2 117 3 3 1 1 1 2 5 4 1 1 2 2 1 2 1 1 1 1 1 1 2

33 1 5 169 4 2 3 1 3 2 3 1 2 8 2 2 1 1 2 1 1

17 2 5 54 1 139 3 3 4 2 1 1 1 4 2 2 3 5 2 1 3 1 5 1 1 1 1 1 1 1 1 11

65 1 1 1 123 1 4 2 1 1 2 1 2 4 1 1 1 2 2 1 1

5 1 7 2 5 1 1 1 1 1

12 1 1 1 35 2 1 2 1 1 1 2 1 1 2 1 1 2 1

2 1 2 1

2 1 1 95 1 6 5 1 1 1 3 1 6 2 6 1 1 3 4 1 1 2 1

4 1 1 18 1 1 1 1 1 2 1 1

35 1 1 1 132 1 1 3 2 2 18 2 2 8 3 1 1 1 1 1 2 1 1 1 1 1 3

58 2 1 2 1 5 1 2 9 1 2 1 1 4 1 1 2 15 1 6 1 1 1 1 1 1 1 2 1 1 1 1

8 1 3 1 34 1 1 1 2 1

16 2 15 3 2 2 1 2 1 1 1 6 3 2 1 1 5 5

73 3 1 93 2 1 5 51 1 1 1

222 2 2 95 3 1 1 2 3 1 1 2 1

14 1 1 1 239 1 1 1 1 2 3 1

21 3 4 24 3 1 2 1 3 1 1 1 16 12 4 1 1 1 2 1 3 2 1 1

51 3 2 1 63 1 2 3 1 2 3 25 1 1 19 1 13 2 4 1 1 1 2 1 1 1 5

13 2 1 1 298 1 1 1 1 1 1 1 4 1 4 1 1 1 2 1 1 1 2

44 3 1 93 1 4 5 1 79 4 5 4 1 1 2 2 1 1 1 1 1

33 7 1 2 1 73 1 1 1 6 2 22 1 28 7 1 1 1 1 2

55 1 1 22 4 1 2 1 1 1 7 1 9 11 2 1 1 1 1 1 1 1 1

168 2 77 2 2 1 1 4 1 21 14 1 1 1 1 9 1 1

8 6 1 1 3 1 1 1 2 1 1

48 1 8 1 11 2 3 3 2 1 2 2 45 1 2 16 2 5 1 1 2 5 3 1 1 2 1 4 11

67 3 1 1 3 17 3 1 1 2 3 2 1 14 1 2 5 6 2 1 2 1 1 1 1 1 7

18 2 2 13 127 1 2 11 1 1 18 1 1 5 4 4 1 2 6 1

4 1 282 4 1 2 1 1 1 3 1 4 1

33 1 1 259 15 1 1 1 1 2 2 1

17 3 1 38 1 1 2 3 1 1 1 1 1

3 4 25 4 1 2 1 1 1 1 1 1 1

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6 1 166 1 1 2 3 2 1 4 1

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13 1 1 96 2 1 1 3 1 1 1 1 3 1 1 3 2 1

16 1 3 2 1 1 1 1 2 2 1 1 3 3 2 1

27 5 1 1 23 1 1 3 1 1 1 2 2 5 1 1 1 3 1 1 3 3 1 2 1 4 1 2

3 2 3 12 3 1 1 1 3 1 1 2 2 1 1 2 1 1 1

43 3 1 174 3 1 1 2 2 4 3 1 1 1 1 2

18 2 6 52 1 1 6 3 1 1 5 1 2 1 7 1 1 1 5 1 1 2 3 1 4 1 1 1 1 1 1

33 11 1 221 1 4 1 11 2 2 1 5 1 1 1 6 1 3 7 1 1 1 1 1

37 3 1 134 3 1 5 3 3 2 1 3 7 1 1 6 1 1 1 3 3 1 1 1

45 4 1 172 1 6 1 2 1 1 3 17 22 4 3 4 4 4 2 1 1 2 1 1

11 3 221 5 1 1 3 3 5 1 4 2 4 3 1 1 1

43 1 12 2 171 1 7 2 1 1 6 1 2 3 1 7 13 1 1 2 3 3 1 2 1 2 1 3 22 3 2 1

112 4 1 1 98 1 2 2 6 1 2 29 11 3 1 1 1 1 3 1 2 24 1 1 1

113 4 158 1 2 4 4 1 1 14 6 1 1 1 3 3 8 1 1 2 1

2 4 1 183 3 2 1 2 1 2 5 1 3 3 3 1 1 1 1 1 1 1 4 1 1

24 2 4 24 3 4 3 6 1 1 1 1 1 4 2 1 1 2 4 3 2 6 1 1

57 3 1 115 4 2 4 1 4 1 1 1 3 1 8 1 1 3 2 2 2

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27 2 1 1 135 3 3 1 1 1 3 1 1 2 2 3 1 1 1 1 2 1 1 1 1 4 1 2 2 1 7 1 1

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165 1

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57 4

82 11

25 17

336

266

332 5

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352 2

277 17

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324 14

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299 13

316 4

285 9

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188

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137 4

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181 1

333 5

21 4

12 1

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48 1

291 6

238 3

175 1

249 11

28 4

37 3

181 1

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87 6

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208

131

138

216

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336

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110

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341

255

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187

150

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306

318

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41

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243

133

318

223

303

270

322

310

330

229

102

217

316

216

50

257

142172

273

198

90120

403

280

225

174

232

24

33

88

43

70

Spores And Pollen

Samples

Sam

ple

sin

Dis

cip

line(s

):

Paly

2.46 PPM-1 26

9.16 PPM-1 32.7

18.46 PPM-1 42

28.39 PPM-1 51.93

36.46 PPM-1 60

48.71 PPM-1 72.25


154.36 PPM-2 109.9

165.96 PPM-2 121.5

178.46 PPM-2 134

190.76 PPM-2 146.3

202.46 PPM-2 158

214.86 PPM-2 170.4

226.46 PPM-2 182

238.86 PPM-2 194.4

250.76 PPM-2 206.3256.86 PPM-2 212.4

268.56 PPM-2 224.1

281.21 PPM-2 236.75

293.51 PPM-2 249.05

306.66 PPM-2 262.2

317.46 PPM-2 273

324.46 PPM-5 32

336.56 PPM-5 44.1

348.46 PPM-5 56

361.26 PPM-5 68.8

370.91 PPM-5 78.45

380.46 PPM-5 88

392.76 PPM-5 100.3

404.46 PPM-5 112

417.96 PPM-5 125.5

429.46 PPM-5 137

452.46 PPM-5 160

464.51 PPM-5 172.05

476.61 PPM-5 184.15

508.46 PPM-5 216

522.96 PPM-5 230.5

535.46 PPM-5 243

545.46 PPM-5 253

560.06 PPM-5 267.6

572.46 PPM-5 280

632.46 PPI-3 9.1

643.36 PPI-3 20

651.36 PPI-3 28

661.66 PPI-3 38.3

671.36 PPI-3 48

679.36 PPI-3 56

691.36 PPI-3 68

707.36 PPI-3 84711.06 PPI-3 87.7

723.06 PPI-3 99.7

731.36 PPI-3 108

745.06 PPI-3 121.7

751.36 PPI-3 128

763.36 PPI-3 140

771.36 PPI-3 148

784.46 PPI-3 161.1

795.36 PPI-3 172

807.36 PPI-3 184

819.36 PPI-3 196

831.46 PPI-3 208.1

843.36 PPI-3 220

855.36 PPI-3 232

867.36 PPI-3 244


Scale : 1:2500

Depth

50m

100m

150m

200m

250m

300m

350m

400m

450m

500m

550m

600m

650m

700m

750m

800m

850m

Text Keys*1 Longapertites proxapertitoides var proxapertitoides


Zo

ne C

Zo

ne B

Zo

ne A

APPENDIX F. in the Umir Formation, San Luis Area, Middle Magdalena Valle Basin (MMVB)Quantitative distribution of palynomorphs

72

73

APPENDIX G ILLUSTRATIONS OF SELECTED TAXA IDENTIFIED IN THE UMIR FORMATION.

7574

PLATE 1

1 Laevigatosporites granulatus. Sample PPM-1 85.8 m, EF F25

2 Striamonoletes sp. Sample PPI-244 m EF W42

3 Psilatriletes group Sample PPM-5 280 m EF M23

4 Psilatriletes group Sample PPM-5 280 m EF G25

5 Kuylisporites waterbolkii Sample PPM-2 146.3 m EF N23

6 Polypodiisporites sp. Sample PPM-1 160 m EF W53

7 Ariadnaesporites sp. Sample PPM-5 280 m EF W26

8 Chomotriletes minor Sample PPM-5 216 EF O16

9, 10. Echitriletes sp. Sample PPM-1 143 EF J16

11, 12 Rugulatisporis sp. Sample PPM-5 125,5 m EF G30

13, 14 Clavatriletes mutisii Sample PPI-3 140 m EF R20

15, 16 Fovetriletes margaritae Sample PPM-1 26 EF H56

17 Gabonisporis vigorouxii PPI-3 161,1 m EF H25

75

1 2 3 4

5

6 7

8

9

1013

16

11

12

17

20 µm

14

15

7776

PLATE 2

1,2 Hamulatisporis caperatus. Sample PPM-1 124 m, EF V31

3,4 Polypodiaceoisporites sp. Sample PPM-2 m EF N51

5,6 Verrutriletes “macrogemmatus”, Sample PPI-3 128 m EF F46

7,8 Cingulatisporis verrucatus Sample PPM-5 160 m EF K99

9 Echitriletes intercolensis Sample PPM-5 126.5 m EF D12

10, 11 Echitriletes intercolensis Sample PPM-5 172.05 m EF Q52

12,13 Muerrigerisporis “ardilensis” Sample PPI-3 184 m EF N11

14, 15 Neoraistrickia “constrictus” Sample PPI-3 220 m EF R47

16. Cicatricosisporites sp. Sample PPI-1 220 m EF M19

17 Echitriletes “acanthotriletoides” Sample PPI-3 161,1 m EF Q11

18 Scabratriletes granularis Sample PPM-2 170.4 m EF Q24

19 Zlivisporis blanensis Sample PPM-1 51.93 EF O56

20 Magnopsilatriletes “magnovirueloides” PPI-3 244 m EF H19

21 Verrutriletes virueloides PPI-3 84 m EF M25

77

20 µm

3 4

14

15

1110

7

1716

21

18

19

20

21

5

6

9

12 138

78

PLATE 3

1,2 Araucariacites australis. Sample PPI-3 220 m, EF H21

3,4 Retipollenites “afropollensis”. Sample PPI-3 244 m EF Y52

5 Arecipites regio, Sample PPM-1 133.2 m EF U41

6 Arecipites regio, Sample PPM;5 100.3 m EF U9

7,8 Cycadopites sp. Sample PPM-5 253 m EF R45

9 Callialasporites dampieri. Sample PPI-3 161.7 m EF W47

10 Monocolpopollenites sp. Sample PPM-5 100.3 m EF L45

11 Monocolpopollenites sp. Sample PPM-5 100.3 m EF P9

12 Retimonocolpites retifossulatus Sample PPI-3 100.3 m EF R18

13 Retimonocolpites retifossulatus Sample PPI-3 125.5 m EF H12

14 Rugomonocolpites “perfectus” Sample PPI-3 184 m EF U8

15 Baculamonocolpites sp. Sample PPM-5 253 m EF E39

16 Foveomonocolpites “heterofoveolatus” sp. Sample PPM-1 160 m EF E49

17 Bacumorphomonocolpites tausae Sample PPI-3 161,1 m EF M25

18 Bacumorphomonocolpites tausae Sample PPI-3 161,1 m EF P23

79

1

2 3 4

5

9

8

11

13 14

17 18

15

16

10

12

6

7

20 µm

8180

PLATE 4

1 Echimonocolpites protofranciscoi. Sample PPI-3 161.1 m, EF N35

2, 3 Echimonocolpites pachyexinatus. Sample PPM-1 23.54 m, EF V59

4,5 Gemmamonocolpites dispersus. Sample PPM-1 92.05 m EF U57

6 Longapertites vanendeerburgi. Sample PPM-1 60 m EF T55

7 Lonagapertites sp. Sample PPM-1 51.93 m EF N10

8 Longapertites proxapertitoides var. proxapertitoides. Sample PPI-I 244 m EF

G10

9 Longapertites proxapertitoides var. proxapertitoides. Sample PPM-1 133.2 m

EF E42

10 Proxapertites verrucatus. Sample PPM-1 92.05 m EF J30

11 Proxapertites verrucatus. Sample PPM-1 92.05 m EF W24

12 Monocolpites grandispiniger. Sample PPM-2 224.1 m EF U27

13 Proxapertites verrucatus. Sample PPM-2 158 m EF Q12

14 Proxapertites “diminutus”. Sample PPM-2 41 m EF M16

15 Proxapertites operculatus. Sample PPM-2 41 m EF R20

16 Proxapertites humbertoides. Sample PPM-1 51.93 m EF V20

81

20 µm

12 3

4

5

7

8

6

9

10 11

12

13

14

15 16

82

PLATE 5

1,4 Spinizonocolpites baculatus. Sample PPM-5 230.5 m, EF M11

2, 3 Spinizonocolpites intrarugulatus. Sample PPM-1 115.25 m, EF W53

5 Spinizonocolpites “clavatus”. Sample PPM-1 115.25 m EF H51

6 Spinizonocolpites “clavatus”. Sample PPM-5 88 m EF S14

7 Spinizonocolpites “clavatus”. Sample PPM-5 276.5 m EF J26

8, 9 Spinizonocolpites “brevibaculatus”. Sample PPM-5 267.6 m EF J21

10, 11 Retidiporites magdalenensis. Sample PPM-5 253 m EF W8

12, 13 Retidiporites botulus. Sample PPM-5 112 m EF H57

14, 15 Psilamonocolpites operculatus. Sample PPM-5 243 m EF P49

83

22

20 µm

1 2 3

4

5

7 8

65

9

10 11 12 1314 15

84

PLATE 6

1,2 Aquilapollenites magnus. Sample PPM-5 172.05 m, EF S51

2, 3 Aquilapollenites sp. Sample PPM-1 92.05 m, EF C42

5 Foveotricolpites hammeni. Sample PPM-1 104.5 m EF R7

6 Foveotricolpites hammeni. Sample PPM-5 230.5 m EF P22

7, 8 Psilabrevitricolpites marginatus. Sample PPM-5 216 m EF U46

9 Annutriporites iversenii. Sample PPM-2 146.3 m EF G8

10 Annutriporites iversenii. Sample PPM-1 92.05 m EF H17

11 Syndemicolpites typicus. Sample PPM-1 42 m EF U25

12 Syndemicolpites typicus. Sample PPM-2 230.15 m EF U12

13 Psilabrevitricolporites annulatus. Sample PPM-5 253 m EF N39

14, 15 Scabrastephanocolpites guaduensis. Sample PPM-5 100.3 m EF W46

16 Retibrevitricolpites brevicolpatus. Sample PPI-3 140 m EF U39

17 Retibrevitricolpites brevicolpatus. Sample PPM-5 100.3 m EF Q49

18 Echitriporites trianguliformis. Sample PPM-5 253 m EF F55

19 Echitriporites suescae. Sample PPM-1 92.05 m EF N23

20 Echitriporites suescae. Sample PPM-1 143 m EF S24

85

20 µm

1 2

3

4

57 8

6

9

10

11

12

13 14 15

1716

2018 19

19

86

PLATE 7

1 Proteacidites dehaani. Sample PPM-1 104.5 m, EF W10

2 Proteacidites dehaani. Sample PPM-5 184.5 m, EF Q22

3,4 Horniella lunarensis. Sample PPM-1 51.93 m, EF T58

5, 6 Retitriporites “crassoreticulatus”. Sample PPI-3 38.3 m EF E41

7 Retitricolpites josephinae. Sample PPM-1 51.93 m EF M16

8 Retitricolpites josephinae. Sample PPI-3 140 m EF R10

9 Retitricolpites josephinae. Sample PPI-3 232 m EF F15

10, 11 Retritricolpites “operculoesponjosus”. Sample PPI-3 161.1 m EF R11

12 Psilatricolporites “scabratus”. Sample PPM-5 88 m EF O50

13 Zonotricolpites variabilis. Sample PPM-2 41 m EF T16

14, 15, 16 Syncolporites lisamae. Sample PPM-1 60 m EF G17

17, 18, 19 Syncolporites lisamae. Sample PPM-1 85.8 m EF P46

20 Syncolporites marginatus. Sample PPM-1 60 m EF M31

21, 22 Colombipollis tropicalis. Sample PPM-1 42 m EF X10

87

1 2

20 µm

3

4

5

6

7

9

810

11

12

13

14

17

15

18

16

19

20 21

22

88

PLATE 8

1 Crusafontites grandiosus. Sample PPI-3 224 m, EF T22

2,3 Retistephancolpites minimus. Sample PPI-3 140 m, EF S6

4 Retistephanocolpites “jandufourioides”. Sample PPM-5 68.8 m, EF O43

5 Retistephanocolpites “jandufourioides”. Sample PPM-5 267.6 m EF 239

6 Stephanocolpites costatus. Sample PPM-1 42 m EF U25

7 Stephanocolpites costatus. Sample PPM-2 41 m EF S54

8 Echistephanocolpites “minutiechinatus”. Sample PPM-5 253 m EF S42

9 Echistephanocolpites “minutiechinatus”. Sample PPM-5 253 m EF U48

10 Buttinia andreevi. Sample PPI-232 140 m, EF Q52

11 Buttinia andreevi. Sample PPM-2 224.1 m, EF O54

12, 13 Periretisyncolpites giganteus. Sample PPM-2 224.1 m EF K39

14 Periretisyncolpites baculatus. Sample PPM-5 160 m EF N29

15 Periretisyncolpites magnosagenatus. Sample PPM-2 244.1 m EF K45

Periretisyncolpites giganteus. Sample PPM-2 224.1 m EF K39

89

20 µm

1

2

3 4 5

6

7

8

9

10 11

12 13

14 15

90

PLATE 9

1 Andalusiella gabonensis. Sample PPM-5 172.05 m, EF O46

2 Andalusiella polymorpha. Sample PPM-1 42 m, EF O26

3 Andalusiella polymorpha. Sample PPM-1 42 m, EF V17

4 Andalusiella rombhoides. Sample PPM-1 42 m, EF V14

5 Andalusiella sp. Sample PPM-1 42 m, EF Q28

6 Andalusiella mauthei. Sample PPM-1 42 m, EF U11


8 Andalusiella mauthei. Sample PPM-1 42 m, EF U52 Phase Contrast

9 Andalusiella polymorpha. Sample PPM-1 42 m, EF K27

91

40 µm1

2 3

4 5 6

7 8 9

92

PLATE 10

1 Andalusiella sp. Sample PPM-1 42 m, EF X15

2 Andalusiella sp. Sample PPM-1 42 m, EF X15 Phase Contrast


4 Palaeocystodinium australinum. Sample PPM-1 42 m, EF S12

5 Palaeocystodinium australinum. Sample PPM-1 42 m, EF S12 Phase Contrast

6 Palaeocystodinium golzowense. Sample PPM-1 160 m, EF F11

7 Andalusiella rombhoides. Sample PPM-2 224.1 m, EF H10/2

8 Cerodinium diebelii. Sample PPM-5 137 m, EF P27

9 Cerodinium diebelii. Sample PPM-5 137 m, EF P27

93

40 µm

1 2 3

4 5 6

7 8 9

94

PLATE 11

1 Manumiella seelandica. Sample PPM-1 42 m, EF U53

2 Manumiella seelandica. Sample PPM-1 42 m, EF U53 Phase Contrast

3 Fibrocysta sp. Sample PPM-1 143 m, EF Q50

4 Alysogimnium euclaense. Sample PPM-1 42 m, EF K23

5 Dinogymnium sp. Sample PPM-5 253 m, EF H11

6 Cerodinium speciosum. Sample PPM-2 97.4 m, EF G13

7 Senegalinium sp. Sample PPI-3 244 m, EF U42

8 Dinogymnium heterocostatum. Sample PPM-2 134 m, EF G38

9 Dinogymnium acuminatum. Sample PPM-5 280 m, EF K12

95

40 µm

1 2

3

4 5

6 7 8

9

96

PLATE 12

1 Achomosphaera sp. Sample PPM-1 51.93 m, EF K22

2 Achomosphaera sp. Sample PPM-1 124 m, EF U27

3 Achomosphaera ramulifera. Sample PPM-2 224.1 m, EF W22

4 Hystrichokolpoma sp. Sample PPM-1 51.93 m, EF Q19

5 Cordosphaeridium sp. Sample PPM-1 60 m, EF Q60

6 Hystrichokolpoma bulbosum. Sample PPM-1 51.93 m, EF P16

7 Hystrichokolpoma bulbosum. Sample PPM-1 51.93 m, EF P16

8 Dinogymnium heterocostatum. Sample PPM-2 134 m, EF G38

9 Foram lining. Sample PPI-3 184 m, EF G20

97

40 µm

1 2

3 45

6 7 8

98

PLATE 13

1 Areoligera senonensis. Sample PPM-2 224.1 m, EF Q19

2 Areoligera senonensis. Sample PPM-2 224.1 m, EF Q19 Phase Contrast

3 Florentinia mantellii. Sample PPM-2 224.1 m, EF Y21

4 Florentinia mantellii. Sample PPM-2 224.1 m, EF Y21

5 Florentinia sp. Sample PPM-1 196 m, EF U43

6 Hystrichodinium sp. Sample PPM-1 85.8 m, EF X26

7 Hystrichokolpoma sp. Sample PPM-1 42 m, EF Q16

8 Exochosphaeridium sp. Sample PPI-3 184 m, EF I38

99

40 µm

1 2

3

4

5

6 78

100

VITA

Carlos Santos was born in Bucaramanga, Colombia. He received a Bachelor of Science degree in

Geology from the Universidad Industrial de Santander in May, 2005. Following graduation, he

worked as a junior palynologist during 2005-2010 in the Colombian Petroleum Institute. In 2010

he was accepted for graduate studies at the Department of Geology and Geophysics at Louisiana

State University, where he was held a graduate teaching assistantship for the period August 2010

to December 2011 and a educational curatorial assistantship from the LSU Museum of Natural

during January –May 2012.

Upon completion of his MS program in spring 2012, Carlos will be working in the Colombian

Petroleum Institute.

palynostratigraphy of the umir formation ...palynostratigraphy of the umir formation, middle...

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