fossiliferous wackestone mancini etal 2005

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505Gulf Coast Association of Geological Societies Transactions, Volume 55, 2005

Potential Reef-Reservoir Facies: Lower Cretaceous Deep-Water

Thrombolites, Onshore Central Gulf Of Mexico

Mancini, Ernest A.;

1

Llins, Juan Carlos;

1

Scott, Robert W.;

2

and Llins, Ruben

3

1Center for Sedimentary Basin Studies andDepartment of Geological Sciences, Box 870338, Tuscaloosa,

Alabama 35487-03382Precision Stratigraphy Associates and Tulsa University, RR 3, Box 103-3, Cleveland, Oklahoma 740203Independent Consultant, Cra. 13A # 89-38 of 504, Bogot, Colombia

Abstract

Upper Jurassic (Oxfordian) thrombolite boundstone and doloboundstone are proven hydro-

carbon reef reservoirs in the onshore northeastern Gulf of Mexico. These Oxfordian thrombolite

buildups attained a thickness of 190 ft (58 m) and are as much as 2.4 mi2 ( 6.2 km2) in area. They

developed in a shallow water setting in less than 30 ft (10 m) of water. Thrombolite buildups alsooccur in Lower Cretaceous (Berriasian to Barremian) strata in the onshore central Gulf of Mexico.

A representative thrombolite is observed in the well log signatures and core samples from the

Lawrence L. McAlpin #1 well, Vernon Parish, Louisiana, which attains a thickness of 35 ft (11 m).

Seismic data show that this thrombolite buildup developed in a fore-reef slope setting in up to 300

ft (90 m) of water on the upper part of the continental slope. The thrombolite boundstone has a

micritic fabric and is interbedded with fossiliferous wackestone. Although this thrombolite bound-

stone facies could have high reservoir potential where dolomitized, the geographic distribution of

this facies has not been delineated. These thrombolites were formed by eurytopic organisms, which

were not restricted by water depth, salinity, temperature, or light penetration. Their origin and

growth typically corresponded to times of rising sea level under low background sedimentation

rates and low-energy conditions. The demise of the thrombolites resulted from the development of

stenotopic, higher-energy paleoenvironmental conditions that supported metazoan communities.

These conditions are associated with times of reduction in the rate of sea-level rise.

Introduction

Microbes are abundant and widespread in carbonate and siliciclastic sediments (Riding and

Awramik, 2000). They are microscopic and include bacteria, algae, fungi and protozoans. They range in

geologic age from the Proterozoic to the present (Riding, 1991; Leinfelder and Schmid, 2000).

Kennard and James (1986) proposed a field classification of lower Paleozoic microbial structures

based on the dominant type of constructive mesoscopic constituents (Fig. 1). The three end members in

this classification were stromatolites, thrombolites, and undifferentiated microbial boundstone. Stroma-

tolites (Fig. 2A) were described as laminated organosedimentary structures built by episodic sediment-

trapping, sediment-binding and/or carbonate-precipitating activity of microbial communities. Thromb-

olites were described as lacking lamination and characterized by a mesoscopic clotted fabric (Fig. 2B).Braga et al. (1995) classified the microbial boundstone as structureless and dense (leiolite).

Thrombolites have been recognized in the Upper Jurassic of the northern Gulf of Mexico by

Baria et al. (1982), Crevello and Harris (1984), Powers (1990), Markland (1992), Benson et al. (1996),

Kopaska-Merkel (1998, 2002), Hart and Balch (2000), Mancini et al. (2000), Parcell (2000, 2002,

2003), Mancini and Parcell (2001), Llins (2002, 2003, 2004), and Mancini et al., (2004). Baria et al.

(1982), Powers (1990), Markland (1992), and Benson et al. (1996) described these Upper Jurassic

buildups as blue-green algal. Crevello and Harris (1984) referred to these buildups as stromatolitic algal

mounds dominated by laminated stromatolites with pelleted thrombolite growth forms. Mancini et al.

(2000) described these as cyanobacterial. Parcell (2000), Mancini and Parcell (2001), and later authors

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Potential Reef-Reservoir Facies: Lower Cretaceous Deep-Water Thrombolites, Onshore Central Gulf Of Mexico

506

Figure 2. Core photographs of microbial textures: (A) stromatolite found in Vocation Field, Mon-

roe County, Alabama, well Permit #3739 at a depth of 14,066 ft (4,287 m), and (B) thrombolite

buildup in Little Cedar Creek Field, Conecuh County, well Permit #13472 at a depth of 11,553 ft

(3,521 m).

referred to these buildups as thrombolitic. Lower Cretaceous thrombolite mounds are well developed

both on the platform margins and on the upper slope in northern Spain (Garca-Mondjar and Fernn-

dez-Mendiola, 1995).

The purpose of this paper is to characterize Lower Cretaceous (Berriasian to Barremian) pre-

Sligo (Hosston) thrombolite buildups from the subsurface of west-central Louisiana. These buildups

were observed in core from the Lawrence McAlpin #1 well, Vernon Parish, Louisiana (Fig. 3A).

Figure 1. Microbial textures: Classifica-

tion of microbial textures is based onthe dominant type of constructive meso-

scopic constituents proposed by Ken-

nard and James (1986) and Braga et al.

(1995).

Stromatolites Leiolites

Thrombolites(clotted)

(dense)(laminated)

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Mancini et al.

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Figure 3. Lawrence L. McAlpin #1 well , Vernon Parish, Louisiana, (A) Location map including the position of

the Aptian shelf margin, and (B) South-North migrated seismic section with the location of the McAlpin well

and illustrating the Upper Cretaceous, Albian, and Aptian shelf margins. Notice the progradation of the pre-Aptian shelf margin expressed by high amplitude south-dipping reflectors (modified from Tyrrell and Scott,

1987). TBI = Lower Cretaceous thrombolite buildup interval.

Thrombolite Characterization

The thrombolite in the McAlpin #1 well was identified in the lithologic core. The suite of logs

available for this well consisted of spontaneous potential (SP) and resistivity (ILD) curves (Fig. 4). No

distinctive pattern was recognized in these curves as indicative of the presence of the thrombolite. How-

ever, there is an interval of approximately 80 ft (24 m) thick, containing the thrombolite buildup and the

beds directly above it, which shows relatively low SP values coupled with high resistivity readings.Above the cored interval, a thick section characterized by low SP values in conjunction with high resis-

tivities, suggests the presence of massive limestone beds. Below the cored interval, the SP curve has a

steady pattern in the high range, while the ILD curve shifts toward lower readings indicating a predomi-

nantly shaley section.

The cored section that includes the thrombolites is 200 ft (61 m) (Fig. 4) and consists largely of

dark gray bioturbated wackestone and mudstone characterized by concoidal fractures. Some thin oncoi-

dal packstone beds are also present. The microbial buildup attains a total thickness of 35 ft (11 m) and

consists of dark gray thrombolite boundstone interbedded with moderately gray wackestone. The

thrombolite buildup shows the characteristic clotted fabric formed by microbial colonies and finely

crystalline carbonate sediment (Figs. 5A, C, and D). A thin breccia (Fig. 5B) is interbedded with the

calci-microbial deposit. The breccia is formed by irregular and angular wackestone fragments floating

in fine grained dark gray micritic matrix rich in fossil fragments. Much of the cored section is moder-ately bioturbated; Thalassinoides andPlanolites burrows are quite common. Wispy organic-rich

laminae and microstylolites are also present. In thin section, the microbial framework consists of a

peloidal texture with diverse types of arrangements (Fig. 6). Very fine calcite crystals (microsparite) fill

the space between the dark peloidal clusters. No open pore spaces were observed. Sparse fossil frag-

ments of echinoids, bivalves, including pycnodont oysters, microsolenid corals, stromatoporoids,

sponge debris, ostracods, and benthic foraminifera, including miliolids, lenticulinids, trocholinids, and

uniserial and biserial foraminifera forms. Thin section analysis reveals a small amount of silt-size terrig-

enous grains (1-3%), which is concentrated in burrows and other interstices and secondary quartz

crystals in matrix and fossils.

0 4 Mi

0 4 Km

SEISCOM DELTA LINE

TIME SECTION

Vernon & Sabine Parishes,Louisiana

Amoco Production Co.

LAWRENCE L. McALPIN1

Upper K.

Albian

Aptian

SN

TBI

Louisiana

LawrenceL.McAlpin #1

AptianShelfMargin

(A) (B)4

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Figure 4. Core description and wireline log for the Lawrence L. McAlpin # 1 well, Louisiana.

EXPLANATION

Oncoid

Nodule

Microstylolites

Thalassinoides

Planolites

Bioturbation

Limestone

Bioclasts &indeterminedshells

Oyster

Echinoids

Stromatoporoids

meters

17750

17725

17700

17675

17650

17625

17550

feet

17600

17575

DEPTH

5410

5400

5390

5380

5370

5360

5350

ms ws ps gs bsDESCRIPTION

Lime mudstone grading upward t o wackestone.

Dark gray lime mudstone, closely spaced concoidalfractures.

Dark gray homogeneous wackestone, rare wispylamination, few fractures.

Moderate to dark gray homogeneous wackestone, localpatches of replacement calcite.

Moderate to dark gray, homogeneous wackestone inter-bedded with oncoidal packstone.

Gray, homogeneous wackestone, stromatoporoidsencrusting indeterminate nodular spar colonies.

Horizontal and long verti cal fractures.

Dark gray thrombolite boundstone with mottled fabricof dark gray irregular hemispherical mud and i nterareas(cavities) of gray argillaceous lime mudstone , wackestoneinterbedded.

Moderate gray homogeneous wackestone.

STRATIG.UNIT

Pre-Sligo(HosstonFormationequivalent)

LAWRENCE L.

Mc ALPIN #1

-50 603 300

MeasuredDepth

(ft)

14500

14000

13500

13000

12500

16000

15500

15000

16500

19050

18500

18000

17500

17000

mV OHMM

SP ILD

SP spontaneous potent ial ILD Long Inducti on Resistivit y

18025

bsmeters

17950

feet

18000

17975

DEPTH

5490

5480

5470

ms ws p s g sDESCRIPTION

Moderate to dark gray, calcareous shale with concoidalfracture, abundant horizontal f ractures.

Lime mudstone grading downward to dark graycalcareous shale, fractures form ing disks.Horizontal fractures increasing in abundance.

Moderate to dark gray, calcareous shale with concoidalfracture, abundant horizontal f ractures.

Dark gray mudstone to wackestone, fractures forming2-10 cm disks, Thalassinoides, sparse horizontal fractures.

STRATIG.UNIT

Pre-Sligo

(TamaulipasFm.)

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Mancini et al.

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f

Figure 5. Core photographs of the thrombolite interval in the Lawrence L. McAlpin #1 well: (A)

17,693 ft (5,393 m), thrombolitic structure with fragments of stromatoporoids and caprinid shells,

(B) 17,697 ft (5,394 m), interbedded brecciated layer formed by irregular wackestone fragments

embedded in a micritic matrix rich in fossil debris, (C) 17,709 ft (5,398 m), non-porous thromb-

olite with the characteristic clotted texture. (Notice that the lighter colored areas correspond to

fine sediment precipitated among the microbial colonies that are expressed by darker colors), and

(D) 17,710 ft (5,398 m), highly, bioturbated thrombolite. (Notice the lack of porosity in the sam-

ples).

(A) (B)

(C) (D)

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Figure 6. Photomicrographs of thrombolitic textures found in the pre-Sligo section of the

Lawrence L. McAlpin #1 well: (A) 17,693 ft (5,393 m), peloidal clusters (dark brown) and

microsparite crystals, (B) 17,697 ft (5,394 m), peloidal clusters are widely separated, (C) 17,710 ft

(5,398 m), peloidal clusters are less defined, (D) 17,710 ft (5,398 m), peloidal clusters with individ-

ual peloids, (E) 17,709 ft (5,398 m), terrigenous silt-size grains within the peloidal clusters, and

(F) 17,709 ft (5,398 m), peloidal clusters amalgamated and individual peloids (Notice the lack of

porosity in the examples).

At a burial depth of 17,700 ft (5,395 m) and with a thickness of 35 ft (11 m), the thrombolite

buildup is not seismically resolvable. However, the seismic interval containing the microbial buildup is

characterized by a change in seismic pattern. Moderately continuous, south-dipping clinoform reflectors

alternating between high and low amplitudes reflect a progradational shelf margin (Fig. 3B). In contrast,

the shallow shelf seismic facies above the slope buildup facies are horizontal, discontinuous, with mod-

erate amplitudes suggesting a lithologic variation of thick massive limestone beds. Based on seismic

data, the thrombolite buildup developed in a fore-reef setting. The breccias described above ( Fig. 5B)

(A) (B)

(C) (D)

(E) (F)

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might be the result of slumps triggered by gravity, which is a common occurrence in this unstable depo-

sitional setting.

Tyrrell and Scott (1987) reportedNannoconus steinmanni at a depth of 17,550 (5,351 m) ft in the

core. This calcareous nannoplankton species ranges in age from Berriasian to Barremian, which indi-

cates that the thrombolite found in the McAlpin #1 well is age-equivalent to the Hosston Formation.

DiscussionThe Upper Jurassic Smackover thrombolite buildups described from the eastern Gulf Coastal

Plain developed in shallow water environments (below wave base in settings of less than 30 ft (10 m) in

water depth (Mancini et al., 2004). These Upper Jurassic buildups attained a thickness of 190 ft (58 m)

and are as much as 2.4 mi2 (6.2 km2) in area. Based on seismic data, the Lower Cretaceous thrombolites

described from the McAlpin well developed in deeper water (300 ft or 90 m), less oxygenated, fore-reef

slope setting (Fig. 7). In Western Europe, Upper Jurassic bioherms of pure thrombolite occur in normal

marine settings of greater than 230 ft (70 m) and as deep as 1,300 ft (400 m) (Leinfelder and Schmid,

2000; Leinfelder, 2001) (Fig. 7). Therefore, bathymetry is not a limiting factor for thrombolite growth.

However, key factors for thrombolite development have been reported to include depositional condi-

tions inherent to a period of overall rise in sea level and lower energy settings, characterized by a hard

substrate for nucleation, zero to low background sedimentation for initial growth, and low to moderate

sedimentation rate for continued growth to support the calcification process (Leinfelder, 1993). Also,important is a paleoenvironment typified by eurytopic environmental conditions, such as fluctuations in

salinity, temperature, oxygen content and/or nutrient supply that limit the growth of other reefal organ-

isms (Mancini et al., 2004). Based on the well log and seismic data, the Lower Cretaceous thrombolites

are interpreted as being deposited during a transgressive pulse within an overall progradational carbon-

ate shelf margin consisting largely of shale and lime mudstone. Variations in the environmental condi-

tions, including an overall shallowing upward, which provided improved oxygen contents and higher

energy levels, contributed toward the demise of the Lower Cretaceous thrombolite buildups and the

accumulation of a thick interval of massive, shallower water limestone.

Figure 7. Profile of a carbonate shelf margin illustrating the paleogeographic location of thrombolite buildups

in the Upper Jurassic Smackover Formation in the northeastern Gulf of Mexico, in the Upper Jurassic strata

in Spain, and in the Lower Cretaceous strata in the Lawrence L. Mc Alpin #1 well (modified from Leinfelder,

1993, Leinfelder and Schmid, 2000, Mancini et al., 2004).

Exploration Strategies

In the eastern Gulf Coastal Plain, the exploration strategy for drilling a successful wildcat well in

the Upper Jurassic thrombolite reservoir play is to identify and delineate paleohighs (generally base-

ment structures) associated with thrombolite buildups. Although the primary control on reservoir

architecture and geographic distribution of these reservoirs is the fabric and texture of the depositional

facies, diagenesis (chiefly dolomitization and/or leaching) is a critical factor that enhances and creates

reservoir quality. Porosity in these boundstone reservoirs is mostly secondary dolomite intercrystalline

intertidalmicrobial mats

lagoonal microbialoncoids Smackover thrombolite

buildups(GOM)

coral-thrombolitereef

sponge-microbolitemud mound

deeper water microbolitemud mound

90 m (~300 ft)

- O2

aphotic microbolitemud mound

400 m (~1,300 ft)

sea levelthrombolite reef pinnacles

(Spain)

Smackover microbial

oncoids(GOM)

Smackoverstromatolite mats

(GOM)

50 m (~160 ft)

10 m (~30 ft)

Smackover microbiallaminites(GOM) Lower Cretaceousthrombolite

in McAlpin #1 (GOM)

70 m (~230 ft)

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512

and vuggy porosity that overprints primary shelter and fenestral porosity. The lithology of the high qual-

ity reservoirs is thrombolite doloboundstone and leached thrombolite boundstone.

The Lower Cretaceous thrombolites encountered in the McAlpin core do not overlie basement

rocks, but rather these thrombolites probably grew on a localized winnowed surface. Such deeper water

thrombolite development is not unusual. The deeper water thrombolites observed in outcrop in Western

Europe formed pinnacles (Figs. 8A and B) with a height of as much as 52 ft (16 m) that nucleated on

local cemented packstone and grainstone (Fig. 8C). Also, shallow water thrombolite buildups of 25 ft (8m) in thickness have been recently discovered in southwest Alabama (Fig. 2B). These thrombolites

apparently developed on a local hard substrate.

Bioherms attaining a thickness of 98 ft (30 m) and an areal extent of 0.9 mi2 (2.3 km2)are present

in the northeastern onshore Gulf of Mexico(Mancini et al., 2004). Therefore, the presence of a thromb-

olite facies of reasonable developmental thickness is common. The McAlpin well log and core indicate

a thrombolite buildup of 35 ft (11 m).

However, in the McAlpin core, the thrombolite boundstone is not dolomitized or leached, and has

no reservoir quality. The principal issue, therefore, in formulating an exploration strategy for potential

deeper water (slope) pre-Sligo thrombolite reservoirs in the western and central Gulf of Mexico is to

determine where the thrombolite boundstone would be leached and/or dolomitized in this area. Dolo-

mitization processes that improved the reservoir properties of the Jurassic thrombolite buildups (i.e.,brine reflux and evaporative pumping) occur in association with shallow marine environments. How-

ever, hydrothermal dolomitization and late stage dissolution processes have the potential to enhance

porosity in the pre-Sligo rocks. The challenge is, therefore, to identify and delineate thrombolite build-

ups along the Lower Cretaceous shelf margins that have been affected favorably by diagenetic

processes.

Because of the depth of burial of the thrombolite boundstone in this area, natural gas would be

the expected hydrocarbon to be encountered.

Conclusions

A microbial buildup consisting of an alternation of thrombolite boundstone and wackestone has

been recognized in the pre-Sligo (Hosston equivalent) cored section of the Lawrence L. McAlpin #1well located in the onshore central Gulf of Mexico area.

The thrombolite buildup attains a thickness of 35 ft (11 m) and was deposited during a transgres-

sive pulse on the fore-slope of an overall progradational carbonate shelf margin. These microbial

deposits accumulated in about 300 ft (90 m) of water during times of anoxic conditions. The demise of

the buildups was due to a change from deeper and anoxic conditions to a shallower, better oxygenated,

and higher energy depositional environment.

Unlike the reservoir-quality microbial doloboundstone and leached boundstone reef reservoirs

found in the Upper Jurassic Smackover section of the northeastern Gulf of Mexico, the Lower Creta-

ceous thrombolite boundstone is not dolomitized or leached and displays no porosity.

The exploration strategy to find reservoir-quality rocks associated with the Lower Cretaceous

shelf margin is to identify and delineate thrombolite buildups with dimensions comparable to theSmackover buildups, and that have been affected by mesogenetic processes that have resulted in dolo-

mitization and/or leaching of the thrombolite boundstone facies creating adequate secondary porosity.

Acknowledgments

This research was funded, in part, by the U.S. Minerals Management Service. However, opinions,

findings, conclusions, or recommendations expressed herein are those of the authors and do not neces-

sarily reflect the views of the U.S. Minerals Management Service.

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Figure 8. Outcrop photographs of thrombolite-bearing buildups at Arroyo Cerezo, Spain: (A)

overview of the outcrop showing two pinnacle reefs, (B) close up of the smaller pinnacle (left side)

in photograph (A), and (C) close up of the base of the thrombolite pinnacle in photograph (B) and

the encrusted and cemented surface on which the thrombolite growth was initiated. Notice the

thrombolite pillow growth structures in photograph (C).

(A)

(B)

Thrombolite Pillows

Encrusted andCemented Surface

Thrombolite Encrusted andCemented Surface

Thrombolite-CoralReef

Coral-ThromboliteReef

Thrombolite-CoralReef

Coral-ThromboliteReef

(C)

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