PRELIMINARY GEOLOGIC DE CRIPTION

ARKLA EXPLORATION T. P. SCOTT NO.5

June, 1986

Prepared by

Shirley P. Dutton and Rober J. Finley

Bureau of Economic Ge logy w. L. Fisher, Direc or

The University of Texas t Austin Austin, Texas 78713- 508

Prepared for

The Gas Research Inst °tute Contract No. 5082-211 0708

Robert J. Finley - Principal Investigator

INTRODUCTION

Three intervals of the Travis Peak Form tion were cored in the Arkansas

Louisiana Gas Company (Arkla) T. P. Scott No.5 well, Waskom field, Harrison

County, Texas. Core was recovered from 5,~23.0 to 5,865.3 ft, 6,143.0 to i

6,235.9 ft, and 7,413.0 to 7,523.0 ft. The! top of the Travis Peak is at

5,841.5 ft (core depth), so 18.5 ft of carbonat1s from the Sl igo Formation were

recovered in the upper cored interval.

MACROSCOPIC CORE DESC1IPTION

The Travis Peak cores were described U~ing a hand lens and binocular

microscope, and graphic logs of the cores werel made at a scale of 1 inch = 5 ft

(fig. 1). The following features of the coref were noted on the descriptive I

logs: depth, rock type, accessories such as ~yrite, organic matter, and bur-

rows; sedimentary structures; texture (sorting), induration; grain size; rela-

tive amount of carbonate cement; color; and s ecial features such as reservoir

bitumen (solid hydrocarbons) and calcareous nodules (fig. 1). Porosity and

permeability values reported by NL Erco are n41ted on the graphic logs, as are

the depths from which thin sections have been ~ade. Correction factors between

core and log depths are noted for each core interval (fig. 1). The cores

consist of medium to very fine sandstone, muds one, and limestone. Each of the

three cored intervals is described below.

The lowest section of core, from 7,413.0 ,to 7,523.0 ft, conta ins thin red

mudstones (up to 4 ft thick) interbedded wi h sandstones up to 29 ft thick

(fig. 1). The sandstone from 7,438 to 7,467 f has a sharp lower contact with

planar laminations and high angle crossbeds at the base, and it fines upward to

1

a burrowed, muddy sandstone at the top (fig. 1. This sandstone is interpreted

to be a fluvial-channel deposit. The middle t upper part of the sandstone is

poorly indurated and in places can be broken into individual sand grains by

hand. This zone is quite porous and permea 1e (porosity as high as 18.9%,

permeabi1 ity as high as 129 md) compared to ost Travis Peak sandstones. As

will be discussed in the section on Petrograph c Description, the detrital sand

grains in this interval are coated by thick rOms of illite that inhibited the

later nucleation of cements, particularly qua tz, and thus preserved much of

the original depositional porosity. This san stone is overlain by a red mud-

stone that contains root traces and has the mo t1ed texture of a soil zone.

The rocks in the lowest section are interpreted to have been

deposited in a fluvial environment. The cr~ssbedded and planar-laminated I

sandstones may be longitudinal and transver e-bar deposits and channel fills

from a sand-rich, low-sinuosity braided stream system. The tops of many of the

sandstones are burrowed, which probably took place after the waning of flood

events. The mudstones interbedded with thes sandstones are interpreted as

overbank floodplain deposits. Floodplain dep not common ly preserved

in braided systems, which would explain why udstones are thin and not vo1u-

metrically as important as the sandstones in t is section of the core.

The middle section of core (6,143.0 to 6, 35.9 ft) contains thicker mud-

stones than does the lowest core. The sandstone at 6,175 to 6,193 ft has a

sharp basa 1 contact, and the hi ghest energy s d i mentary structu res (c rossbeds

and parallel to slightly inclined laminae) ccur in the lower part of the

sandstone. The sandstone fines upward, and t e upper part is burrowed. Many

of the burrows at the top of the sandstone a e highlighted by reservoir bi-

tumen. Calcareous nodules are common in the mudstones. Most of the mudstones

are gray, not red, and some contain pyrite ass ciated with organic matter.

2

There is no evidence of marine deposition in the rocks of the middle cored

interval, and they probably represent alluvial or delta-plain sediments.

Sandstone intervals represent small fluvial hannels or crevasse splays de-

posited in the adjacent floodplain. The red an gray mudstones are interpreted

as overbank floodplain deposits. Mudstones ar relatively thick in this core,

suggesting that the streams carried mixed b dload and suspended load, and !

overbank floodplain deposits were preserved inl the system. The gray color of I

some of the mudstones is probably caused byl a high water table, abundant I

i

organic matter, and reducing fluids that moved Ithrough overlying sandstones. I

The shallowest core (5,823.0 to 5,865.3 f ) records the transition from

terrigenous clastic deposition of the Travis P ak Formation to shallow-marine

limestone deposition of the Sligo Formation Sandstones are rare in this

interval (fig. 1). The thin sandstones that a e present are rippled and bur­

rowed, and they contain reservoir bitumen. Re mudstones persist to depths as

shallow as 5,850 ft, which is only 9 ft below he top of the Travis Peak. The

red and gray mudstones and thin, interbedded andstones of this interval are

interpreted to be tidal flat deposits that were periodically exposed subaerial­

ly. The limestones are classified as packstone, which means they are composed

of ske1eta 1 fragments and carbonate mud. Oyster fragments are the most common

skeletal grains, but pelecypod and gastropod shells were also noted. Thin

stringers of terrigenous-clastic mud are commo . within limestone beds.

PETROGRAPHIC DESCRIP~ION

Detailed study of the core is being conducted with a standard petrographic

microscope and with a scanning electron mic oscope (SEM) that includes an

energy dispersive X-ray system (EDX).

3

Gra in Size

Analysis of grain size was accomplished b making grain-size point counts

of thin sections. Fifty grains per slide were measured along their long dimen­

sion, excluding cement overgrowths in order th determine the size of the de-I

trital grains. Mean diameter of sand- and sil -sized grains was calculated for

each sample (Table 1); detrital and authigenic clays were not included in the

ca lcu1ation of mean gra in diameter. I

Most sand grains are fine or very fi~e, between 0.063 and 0.25 mm,

although some of the grains in the 7,450-ft sa~dstone are medium sand, between !

0.25 and 0.5 mm (Table 1). Most silt is coar e silt, between 0.031 and 0.062

mm. Clay particles are smaller than 0.004 mm.

Mineral Composition

Fifteen thin sections have been point for a preliminary descrip-

tion of mineral composition (Table 2). The sa dstones are mineralogically very

mature, and all but one are classified as quartz arenites. (One sample is a

subarkose.) Quartz comprises 94.4% to 100% f the essential framework con­

stituents (quartz, feldspar, and rock fragment Plagioclase feldspar is more

abundant than orthoclase, and total feldspar volume varies from 0% to 4.7%.

Rock fragments, mainly chert and low-rank met morphic rock fragments, consti­

tute between 0% and 3.7% of the framework grai s.

Au t h i g e n icc em e n t s con s t it ute bet wee n 4.5 % and 27.5 % 0 f the san d s ton e

volume in these 15 samples (Table 2). Authi enic quartz, illite, chlorite,

kaolinite, iron-bearing calcite, dolomite, an erite, anhydrite, and reservoir

bitumen have all been observed in Ark1a Scott No.5 cores.

One of the distinctive features of the Ar 1a Scott samples is the presence

of thick illite cutans around detrital grains in the 7,450-ft sandstone. The

4

upper part of the sandstone (7,442 to 7,453 ft) is porous and poorly indurated,

whereas the lower part (7,453 to 7,462 ft) is ell indurated. Samples in the

upper part contain as much as 14% by volume f clay cutans around detrital

grains and volumes of quartz overgrowths as low as 0.5% (Table 2). The deeper

part of this sandstone has much thinner clay rims (1% to 3%) and correspond­

ingly more quartz cement (15%: Table 2). The cutans are birefringent and are

composed mainly of illite, but EDX analysis of IS EM samples'indicates that some

chlorite occurs in the rims as well. In the upper part of the sandstone, the I

clays form a coat about 2 ~m thick over all th4 detrital grains (fig. 2); where

framework grains have been removed by pluckinglduring thin-section preparation I

or by dissolution of feldspars during burial diagenesis, the thick illite

cutans remain intact and uncrushed (fig. 3).1 Such extremely thick illite i

cutans have not been observed in other Travis Peak samples. The presence of

these cutans apparently inhibited the nucleatio of later cements, particularly

quartz. Thus, the poor induration of this unusual Travis Peak sandstone is

caused by the presence of thick illite cutan and the corresponding lack of

other authigenic cements. The cutans may be th cause of the unusually high SP

and low resistivity log responses in this zone.

The depositional setting of this sandst ne and the distribution of the

cutans within the sandstone suggest that most of the clay entered the sandstone

by mechanical infiltration from the soil above. This process is characteristic

of the vadose zone; downward percolating rain- r floodwater carries clay-sized

material that is deposited tangentially to det ital sand grains when the water

evaporates or diffuses into capillaries (Molen ar, 1986). During burial dia-

genesis, the clays may have been altered, for xamp1e to higher crystallinity.

Authigenic illite and chlorite also oc ur as pore-filling cements in

secondary pores that formed by the dissolution of feldspars. Unlike the illite

5

cutans, these cements formed relatively la e in the burial history of the

Travis Peak. Kaolinite cement was observed in primary pores in the Arkla Scott

No.5 samples. Petrographic evidence is equi ocal, but the kaolinite appears

to have precipitated at about the same time as the quartz overgrowths.

Quartz cement is the most abundant authi enic mineral in the Arkla Scott

No.5 cores. Quartz overgrowths fill as much as 23% of the sandstone volume

(Table 2), and precipitation of authigenic qua tz occluded much of the primary

porosity. Where volumes of quartz cement are relatively low, perhaps because

nucleation was inhibited by early illite cu ans, primary porosity has been

retained (Table 2). The sandstone at 6,175 to 6,193 ft has porosities as high

as 21% and permeabilities as high as 52 md fig. 1). Primary porosity in a

sample from 6,187.3 ft can easily be seen in S M (figs. 4 and 5); the volume of

quartz overgrowths in this sample is only 11%.

Dolomite, ankerite, and iron-bearing c lcite occur in the Arkla Scott

No.5 cores. Calcite cement was observed 0 ly in the shallowest sample, at

5,843.5 ft, in a sandstone that is interbedde with limestone. Petrographic

relationships suggest that the calcite cemen precipitated after quartz over­

growths. Dolomite and ankerite are also more abundant in the shallower Travis

Peak cores. No dolomite was observed in the eepest section of core (7,413 to

7,523 ft), and ankerite was observed but not counted (and therefore occurs in

volumes less than 0.5%) in only a few sample from the lowest core (Table 2).

Ankerite cement has a maximum volume of 7.5% in the sample from 6,187.3 (fig.

5), and it could cause completion problems (f rmation of an iron-hydroxide gel)

if it is treated with acid. A decrease in d lomite and ankerite with depth

below the top of the Travis Peak has been n ted in several other Travis Peak

cores (Dutton, 1985).

6

Minor amounts of late anhydrite cement were observed in several thin

sections; it was never hit on a point-count tr verse, and therefore must occur

in volumes of less than 0.5%. Anhydrite was 0 served in the core as nodules at

7,428 and 7,435 ft and along a natural fract re at 7,497 ft. Both of these

occurrences also suggest that the anhydrite .wa~ a late,

did not precipitate in the depositional envlro~ment. I

d i agenet i c fea tu re tha t

Solid hydrocarbons (also known as reservtir bitumen or IIdead oil II) occur

mainly in the upper two sections of the corel(fig. 1). No reservoir bitumen

was observed in the lower core during macros~opic examination, but the thin

section from 7,466.5 ft contained reservoir ijitumen (Table 2). Where it is

abundant, reservoir bitumen fills primary poro~ity; petrographic evidence sug­

gests it entered the sandstones after the pre~iPitation of quartz overgrowths !

and ankerite. Preliminary studies of the res$rvoir bitumen suggest it occurs

mainly in the upper Travis Peak (Dutton, 1985~. It appears to have formed by

deasphalting of pooled oil after solution o!f gas into the oil (Rogers and

others, 1974).

Poros i ty

Porosity observed in thin section in the 15 samples varies from 0% to 6.0%

(Table 2). Both primary and secondary pores ar' present, and primary pores are

particularly abundant in samples with thick il ite cutans. Secondary pores are

formed by the dissolution of framework grains, so they are approximately the

same size as detrital grains. However, they c mmonly contain authigenic clays

and fragments of dissolved framework grains, 'particularly feldspar. Porosity

measured by point counting thin sections is ower than porosity measured by

7

porosimeter on adjacent samples because of the presence of abundant micro­

porosity. Microporosity occurs in detrital an authigenic clays (fig. 5); such

porosity generally cannot be seen in thin se tion, but it can be observed by

SEM and is measured by a porosimeter.

8

Table 1. Grain-size distribution in Arkla T. P. Scott No. 5 core

Detrita 1 Authigenic Textura 1 Depth (ft) Mean (rrm) Sand (%) Silt (%) Clay (%) Clay (%) Class*

5,843.5 .069 55.4 40.1 0 4.5 Silty sandstone

6,178.2 .115 91.6 1.9 0 6.5 Sandstone

6,187.3 .104 92.6 1.9 0 5.5 Sandstone

6,192.0 .158 97.0 0 0 3.0 Sandstone

6,204.4 .119 89.3 5.7 0 5.0 Sandstone

6,208.4 .163 97.5 0 0 2.5 Sandstone

6,218.4 .142 90.2 1.8 5.0 3.0 Sandstone

7,444.2 .172 86.0 0 1.5 14.5 Sandstone

7,446.4 .274 89.5 0 0 10.5 Sandstone

7,451.0 .192 83.5 0 0 16.5 Sandstone

7,458.2 .167 93.5 0 0 6.5 Sandstone

7,462.1 .209 96.0 0 0 4.0 Sandstone

7,466.2 .158 96.0 0 0 4.0 Sandstone

7,489.5 .150 94.0 0 0 6.0 Sandstone

7,494.6 .165 97.0 0 0 3.0 Sandstone

*Textural class determined only by detrital grains.

Table 2. Petrographic analyses of Arkla T. P. Scott No. 5 core, .easured in percent.

Depth = 5,843.5 ft 6,178.2 ft 6,187.3 ft 6,192.0 ft 6,204.4 ft Framework Grains

Quartz 68.0 70.5 71.0 77 .0 74.5 Plagioclase 2.5 2.0 3.5 0.5 1.5 Orthoclase 0.5 0.5 0 2.0 1.5 MRF* 0.5 0 0 0.5 0 Chert 0.5 0 0 0 0.5 Clay clasts 1.0 1.0 1.0 0 2.5 Heavy minerals 0 0 0 0 0 Other 0 0 0 0 0

Matrix

Clay-s ized fi nes 0 0 0 0 0

Cellents

Quartz 14.01

13.5 11.0 16.5 14.0 Do lomi te 7.5 0 0.5 0 0

Ankerite 1.0 0.5 7.5 0 0.5 111 i te 4.5 4.0 4.5 1.0 0 Chlorite 0 2.5 1.0 2.0 1.0

2 Solid organic matter 0 3.5 0 0 4.0

Porosity

Primary porosity 0 1.5 0 0.5 0 Secondary porosity 0 0.5 0 0 0 Porosimeter porosity 1.2 no data no data no data 11.7

*Metamorphic rock fragments lIron-rich calcite 2Kaolinite

Page 1 of 3

Table 2 (continued). Petrographic analyses of Arkla T. P. Scott No. 5 core. measured in percent.

Depth = 6,208.4 ft 6,218.4 ft 7,444.2 ft 7,446.4 ft 7,451.0 ft Framework Grains

Quartz 74.0 69.0 79.0 69.0 73.0 Plagioclase 1.5 2.0 0 0.5 1.5 Orthoclase 1.5 0 0 0 0 MRF* 0 0 0.5 0 0 Chert 0 0 2.5 2.5 1.5 Clay clasts 1.0 6.5 2.0 0.5 1.0 Heavy minerals 0 0 0 0 0 Other 0 0 0 0 0

Matrix

Clay-sized fines 0 5.0 1.5 0 0

Cements

Quartz 19.5 6.5 0 . tzt.5 0.5 Do lomite 0 1.0 0 0 0 Ankerite 0 7.0 0 0 0 Illite 1.5 1.0 11.0 8.0 14.0 Chlorite 0.5

2 2.0 3.5 2.5 2.5

Solid organic matter 0.5 0 0 0 0

Porosity

Primary porosity 0 0 0 2.0 4.5 Secondary porosity 0 0 0 0.5 1.5 Porosimeter porosity 11.5 12.1 no data 18.9 no data

*Metamorphic rock fragments 2Kao 1 inite

Page 2 of 3

Table 2 (continued). Petrographic analyses of Arkla T. P. Scott No. 5 core. measured in percent.

Depth = 7,458.0 ft 7,462.1 ft 7,466.5 ft 7,488.5 ft 7,494.6 ft Framewrk Grains

Quartz 12.5 75.5 12.5 77 .5 78.0 Plagioclase 1.0 1.0 a 0.5 0.5 Orthoclase a a a a a MRF* 0.5 a a a 0.5 Chert 1.0 0.5 a 1.0 0.5 Clay clasts 2.5 a a a a Heavy mi nera 1 s a a a 0.5 a Other a a 2.02 a a

Matrix

Clay-sized fines a a a a a

Cements

Quartz 16.0 14.5 23.0 11.5 15.0 Dolomite a a a a a Ankeri te a a a a a III i te 3.0 1.0 1.0 4.0 0.5 Chlorite 3.5 2.5

2 1.0 1.5

2 1.0

2 Solid organic matter a 0.5 0.5 0.5 1.5

Porosity

Primary porosity a 2.5 a 1.5 1.0 Secondary porosity a 2.0 a 1.5 1.5 Porosimeter porosity no data no da ta no data 11.9 9.7

*Metamorphic rock fragments 2Kao 1 inite

Page 3 of 3

REFERENCES

Dutton, S. P., 1985, Petrography and diagene is of the Travis Peak (Hosston)

Formation, East Texas: The Universit of Texas at Austin, Bureau of

Economic Geology, topical report prepare for the Gas Research Institute

under contract no. 5082-211-0708. i'

Molenaar, Niek, 1986, The interrelationship bftween clay infiltration, quartz

cementation and compaction in Lower Gi~etian terrestrial sandstones, i

no. 3, p. 359 - 3 69.

Journal or Sedimentary Petrology, v. 56, northern Ardennes, Belgium:

Rogers, M. A., McAlary, J. D., and Bailey, N. J. L., 1974, Significance of ,

reservoir bitumens to thermal-maturation jstudies, western Canada Basin:

American Association of Petroleum Geolog. sts, v. 58, no. 9, p. 1806-1824.

FI GURE CAPT! ON

Fi gure 1. Descriptive log of core of the Tr'~iS Peak Formation from the Arkla

Scott No.5 w"ell, Harrison County, Texas. Core depths are 5,823.0 to 5,865.3

ft, 6,143.0 to 6,235.9 ft, and 7,413.0 to 7,523.0 ft.

9

EXPLANATION OF

CONTACT Gradational G

Upward fining ~

ROCK TYPE (%)

Mudstone

Siltstone and sandy siltstone (_ ... - I

Sandstone

Planar ___ ~_-'--'-'---",,"\ Mud clast and mud flake (-~ I conglomerate Erosive E

Upward \l coarsening V

Interbedded sandstone ( .... I, siltstone (-"'-1, and

Slightly irregular- Mudstone

1.J'v Ir

....... -. ...... ___ •• _ Coal

• Porosity

STRUCTURES

Trough crossbedding

Planar crossbedding

Cross beds with oversteepened foresets

Indistinct cross - strati fication

. Gently inclined lamination: GI

Gently inclined lamination separated by low-angle discordances

Horizontal lamination

Ripple trough lamination

Planar ripple lamination

Climbing - ri pple lamination

Heavily bioturbated sandstone

"Massive" sandstone: M

Contorted bedding

Graded bedding

v ACCESSORIES v

v? Vertical and horizontal burrows

...... Organic fragments

A " Rootlets

c:" Shells J (1 Mica flakes'

P Pyrite

c Callianassa burrows -v-

TEXTURE

Sorting

VII'S Very poor

p-s Poor

Rounding

o Angular

s-o Subangular

so, Subrounded

, Rounded

m-s Moderately well

.. -s Well

INDURATION

WI Well indurated

I Indurated

IF Indurated but friable

IS Indurated but shaly

RELATIVE CALCITE CONTENT

Slight effervescence

3 Moderate effervescence

5 Strong effervescence

10 Very strang effervescence

COLOR

Abbreviations from Rock­Color Chart, Geological Society of America

Abbreviations from Geological oCiety of America Rock-Color Chart U ed on

Core Descriptions

5R 6/2 5R 4/2

5 YR 6/1 5YR 4/1 5 YR 7/2

5GY 6/1

N7 N6 N5 N4 N3

Pa le red Grayi sh ed

li ght br wnish Brown i sh gray Gray i sh ranc;e

I i I

Green i sh gray

light gr y

gray

pink

Medium 1 ght gray Medium g ay Medium d rk gray Dark gra

FIG U R E 2.

SEM photograph of illite cutans

coating detrital grain. Depth is

7,451.0 ft. Bar length is 100 ~m;

magnification is 200x.

FIG U R E 4.

SEM photograph of euhedral quartz

overgrowths (Q) and primary porosity.

Microporosity within authigenic clays

is abundant. Depth is 6,187.3 ft.

Bar length is 100 ~m; magnification

is 350x.

FIG U R E 3.

SEM photograph of thick illite cutan.

The framework grain has been removed

by dissolution or plucking during

thin-section preparation. Depth is

7,451.0 ft. Bar length is 10 ~m;

magnification is 750x.

FIG U R E 5.

SEM photograph of quartz overgrowths (Q),

ankerite (A), and chlorite (C) cement.

Depth is 6,187.3 ft. Bar length is

100 ~m; magnification is 500x.

•

TS

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FORMATION \('A"iS ~Ak. COUNTY HacCiSQ""

DEPTH

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. ! STRATIFICATION COMMENTS

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t. P. sc..olT 1\)0. S CORE DEPTH ~ __ ~_(i. __ , = __ G-'L- LOG DEPTH @ ~&39 .r~ FORMATION __ ,----'--'--'ro."'--,,=-',-"'s'----'P-"e.,.G......,k_------ -- COUNTY \-\0. rei so..... LOGGED BY oS· Uv...=H-o '" DATE Y. I a (., WELL A~KLA £XI'Lol':.A-TloN

DEPTH

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