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20. Paleomagnetic Constraints on the Age of Lower Cretaceous Cores from Deep Sea Drilling Project Site 535, Southeastern Gulf of Mexico1

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20. Paleomagnetic Constraints on the Age of Lower Cretaceous Cores from Deep Sea Drilling Project Site 535, Southeastern Gulf of Mexico1 20. PALEOMAGNETIC CONSTRAINTS ON THE AGE OF LOWER CRETACEOUS CORES FROM DEEP SEA DRILLING PROJECT SITE 535, SOUTHEASTERN GULF OF MEXICO1 Margaret M. Testarmata, The University of Texas at Austin, Institute for Geophysics, Austin, Texas ABSTRACT Cretaceous deep-water limestones from Site 535 have low intensities of magnetization, but stable inclinations (37.8° ±7.3) that can readily be isolated after demagnetization to 25 oersteds. The magnetic stratigraphy of the studied por- tion (sub-bottom depth 354.0-515.5 m) shows only two reverse samples, which may be the result of misorientation. The micropaleontological dating of this section as Albian to Hauterivian had implied that several reversals from the M anomaly sequence would be observed. The presence of only normally magnetized samples suggests instead that the studied portion is completely within the Cretaceous long normal zone (Santonian to Aptian). Thus the paleomagnetic data indicate that the micropaleontological dates are too old, a contention supported by postcruise ammonite studies. INTRODUCTION l^ Florida j 261 , 300° The Glomar Challenger drilled 6 sites in the south- eastern Gulf of Mexico in the winter of 1980-1981 dur- - - ?/" ing Leg 77 (Fig. 1A). Two of these sites, 535 and 540, 500 f£ were stratigraphically offset so that a fairly complete 24= 38 yV J 7 >540 - section could be obtained from above the inferred mid- 36 539 Cretaceous unconformity (MCU) through Unconformi- *53& ^> ty 2 (Fig. IB). At the deeper site, Site 535, 559.5 m of "^f Cuba 1 22° N //^ Cretaceous deep-water limestones were penetrated, with 88° W 86° 84° 82° 80° recovery averaging 71%. Shipboard paleontologists dat- ed these limestones as ranging from Albian to Late Ber- B riasian with hiatus in the Aptian and Barremian. West East Paleomagnetic measurements were made on part of this core with the objective of correlating the results 20 km with the marine magnetic time scale and further refining the dates provided by broad-ranging fauna. Four hun- dred nine vertically oriented minicores were collected at 0.5-0.8 m spacing from a 361 m portion (sub-bottom T3 depth 154.5-515.5 m) dated as Albian to Hauterivian. MCU This time period includes the early part of the Creta- ceous long normal period and several reversals of the underlying M anomaly sequence. In addition, 20 sam- ples were collected near the base of the core (sub-bottom depths 673.5-696 m), which was dated as early Valan- ginian to late Berriasian. The magnetic directions of these samples could be useful in discerning any Early Creta- × × x""x •xx xxx x x x x x x x ceous plate motion that occurred in the southeastern Figure 1. A. Location of the six DSDP sites drilled on Leg 77 in the Gulf of Mexico. southeastern Gulf of Mexico. B. Schematic seismic section shows stratigraphic relationship between Sites 535 and 540 and the major METHODS AND MEASUREMENTS unconformities, mid-Cretaceous unconformity (MCU), and Un- conformities 1 and 2. NRM Measurements ments, samples were stored in a magnetically shielded Because very low intensities of magnetization (4.9 × room whose ambient field was approximately 100 gam- 10~9 to 2.9 × 10~7 emu/cm3) prevented shipboard mea- mas. Fields in the magnetometer and demagnetizing surements, all samples were measured postcruise with a equipment were less than 5 gammas. cryogenic magnetometer at the University of Texas Insti- The 361-m section was subdivided into two parts, Cores tute for Geophysics. Prior to and during the measure- 18 through 38 (sub-bottom depth 154.5-354.0 m) and Cores 39 through 56 (sub-bottom depth 354.0-515.5 m). 1 Buffler, R. X, Schlager, W., et al., Init. Repts. DSDP, 11: Washington (U.S. Govt. Although the mean inclinations of the natural remanent Printing Office). ' magnetization (NRM) agree for the two portions, the dis- 531 M. M. TESTARMATA tribution of NRM inclinations and intensities differs sig- stored and measured. Although alternating field demag- nificantly (Fig. 2). The upper section has a much lower netization (AF) was attempted on all 20 samples, their standard deviation than the lower section with respect to extremely low intensities made it difficult to isolate a both parameters. One can observe in Figures 3 and 4 that stable remanence. Therefore, no information about Early the actual changes do not occur at a sub-bottom depth of Cretaceous plate motion in the Gulf of Mexico could be 354 m, but rather at approximately 310 m where the inten- extracted. sity range increases and at 400 m where the intensities de- crease significantly and the inclination range widens. The Demagnetization 400 m discontinuity corresponds to a significant Aptian Because of lack of funding, only the lower portion unconformity marked by üthologic changes. Ammonite (Cores 39 through 56) of the long section was demagne- studies (Young, this volume) indicate that the Cretaceous tized. This part was deemed more important because it sedimentary rocks above this depth have been reworked. ranged in age from Albian to Hauterivian and therefore The 20 samples from the base of the core have very should have recorded the transition from the frequent low NRM intensities and widely scattered NRM inclina- reversals of the M anomaly sequence to the Cretaceous tions (Fig. 5). The scatter seems to be largely the result long normal period (see Fig. 6). The upper section, en- of a viscosity experiment conducted with these samples. tirely within the Albian, would have presented an excel- Those samples indicated by A in Figure 5 were stored in lent opportunity to investigate short reversal events within the Earth's field prior to NRM measurement, while the the Cretaceous long normal zone (VandenBerg and Won- others (•) were stored in a field-free environment for ders, 1980; Lowrie et al., 1980) but would not have offered several months. Those stored in the low field space show the reversals necessary to correlate the section with the ma- inclinations close to the value of 41° which was ob- rine magnetic time scale. served for the overlying samples (see Fig. 2). The scatter One hundred eighty samples were demagnetized at 3 among those stored in the Earth's field suggests that to 6 steps between 25 and 300 oersteds (Oe) to isolate these samples have acquired a viscous remanent magne- the stable magnetization. For all but 4 samples, a stable tization, and it points out the need for a field-free space component was readily isolated, usually after demagnet- on the Glomar Challenger where such samples can be ization to 25 Oe. The consistency of the directions of = 40.6± 7.8 /V-229 /V=229 x = 41.3 ± 12.8 /V= 180 0 20 40 3 Inclination (°) Intensity (emu/cm ) Figjjre 2. Distribution of NRM inclinations and NRM intensities for Cores 18 through 38 (upper) and Cores 39 through 56 (lower), lë~ represents mean value with its standard deviation. 532 PALEOMAGNETIC CONSTRAINTS ON AGE OF LOWER CRETACEOUS CORES NRM inclination (°) Core IMRM intensity (emu/cm' Stable inclination (°) Core Intensity (emu/cm ) .-8 7 -45 0 45 90 I0 " 10- -45 0 45 90 10' 10-7 1 : • 18 .j 39 160- • 360- »•* \ 19 * .< 40 # • 4 20 •.* 180- j* 41 1• •<r * 380- 21 •< i •> . 42 i i, 22 '\ 200- : 43 • » * '* . 400- 23 I • • /* J 44 s '•• ••' 24 '•• 220- 45 r *• 25 420- X 46 .' 26 • 1 * * 47 • * E • 27 •* o o 440- •.: * 48 Á 28 • CO \ • • •• *:" 49 260- 29 50 460- • Φ i 30 ' • • 51 280- .y. • 31 ) i ••y* 52 • • • 480- 32 x• Iβ 53 ." / 300- '" f 33 • 54 • ' - . ' ' 4 • 34 • 500^ 55 * 320- 35 • # * Φ 56 ': 36 -45 45 90 10" 10 10" t I Figure 4. Stable inclinations, observed after demagnetization, and NRM 340- "• 37 intensities for samples from Cores 39 through 56. X denotes sam- ples for which no stable inclination was observed. • 38 • »* -45 90 10 acquired during or soon after deposition. Several rock Figure 3. NRM inclinations and NRM intensities as a function of depth magnetic experiments imply that the stable remanence is for all samples from Cores 18 through 38. carried by fine-grained magnetite. Stepwise thermal de- magnetization to 400 °C was conducted on 8 samples magnetization upon further demagnetization (Fig. 7) at- (sub-bottom depths 326-350 m) which had not been tests to the high quality of the data, especially when one subjected to AF demagnetization. In all cases, the inten- considers the low intensities. Figure 8 shows that de- sity of magnetization decreases gradually with tempera- magnetization has tightened the cluster of inclinations ture (Fig. 9). The absence of a marked change near and has lowered the mean to 38° from the NRM value 320 °C precludes pyrrhotite as a significant contributor of 41°. to the remanence. In a second experiment, 7 representa- tive samples, which had already been AF demagnetized, Magnetic Mineralogy were given an isothermal remanent magnetization (IRM) Before the data can be used for dating the core, it in fields up to 5 kOe. The acquisition curve (Fig. 10) is must be ascertained that the stable magnetization was typical for fine-grained (i.e., single domain) magnetite. 533 M. M. TESTARMATA • A Geomagnetic polarity A £ Core 75 From From ~ 680 -• magneto- oceanic a Stage stratigraphic magnetic E AA sections anomalies Co o 76 £ Danian •ó 690 - 29 26 65 CO A 30 A 77 31 27 0 45 Maestrichtian IMRM intensity 32 28 IMRM inclination (°) (x108 emu/cm3) 29 70 Figure 5. NRM inclinations and NRM intensities for twenty samples 30 from the bottom of Site 535. A indicates samples stored in the 31 Earth's field and , samples stored in a field-free space for several months prior to NRM measurement.
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