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Heavy Minerals In Sediments Of Southern California

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Heavy Minerals In Sediments Of Southern California

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Content This dissertation has been microfilmed exactly as received Mic 60-4473 AZMGN, Emanuel. HEAVY MINERALS IN SEDIMENTS OF SOUTHERN CALIFORNIA. University of Southern California/ P h,D ., I960 Geology University Microfilms, Inc., Ann Arbor, Michigan HEAVY MINERALS IN SEDIMENTS OF SOUTHERN CALIFORNIA by Emanuel Azmon A Dissertation Presented to the FACULTY OF THE GRADUATE SCHOOL UNIVERSITY OF SOUTHERN CALIFORNIA In Partial Fulfillment of the Requirements for the Degree DOCTOR OF PHILOSOPHY (Geology) June i960 UNIVERSITY O F SO U T H E R N CALIFORNIA GRADUATE SCHOO L UNIVERSITY PARK LO S ANGELES 7 . CALIFO RNIA This dissertation, written by EtaanuelA?nion_................. under the direction of his....Dissertation Com mittee, and approved by all its members, has been presented to and accepted by the Graduate School, in partial fulfillment of requirements for the degree of D O C T O R O F P H I L O S O P H Y Dean Date.... Jyne.19.6Q.......... DISSERTATION COMMITTEE 'man TABLE OF CONTENTS INTRODUCTION ........................................ METHOD OF STUDY............................. . . . . Selection of Suitable Grain-Size .................. Preparation of the Samples..................... . Mounting of Grains for Petrographic Analysis . • . . Counting the Grains and Accuracy • » .............. GEOLOGY OF THE SOURCE AREAS ........................ Tectonic Provinces .... ........................ Santa Ynez Mountains . . . . . . . . . . . . . . . . Ventura Basin...................................... Santa Monica Mountains ........ ........ .. Los Angeles Basin ................................ Southern California Batholith .................... Continental Borderland .. ........................ Provenance of Heavy Minerals ...................... DISTRIBUTION AND PROVENANCE........................ Heavy Mineral Provinces........................ Province I ...................................... Province II ...................................... Province III ............... ...... ........... Province I V .......... .......................... Trends in Averages........................... . . Percentage of Heavies ............................ Age and Correlation............................ SUMMARY AND CONCLUSIONS........................ . . ECONOMIC GEOLOGY .................................... REFERENCES .......................................... APPENDIXES .......................................... Appendix A. Mineral Identification in Sand . . . . ii Page Appendix B. Station Locations ..................... 115 Appendix C. Heavy Mineral Frequencies in Percent . 131 Appendix D. Averages of Heavy Mineral Frequencies . I*f0 1. Rivers and Rock Outcrops...........I*f0 2. Beaches . ........................... 1*K) 3. Inshore to 50 Fathoms............... l1 ^ * t - . Offshore Past 50 Fathoms........... 1*K) 5. All Environments.............. . 1*K) 6. All Environments Based on 0.8 Per cent Heavy Minerals........... lb-1 Appendix E. M a p s ................................ 1^3 Map I. Heavy Mineral Provinces in southern California . . • • 1**3 Map • H H Heavy Mineral Assemblages Surf to Santa Barbara • • 1^4 Map III. Heavy Mineral Assemblages Santa Barbara to Point Dume Map IV. Heavy Mineral Assemblages Point Dume to Corona del Mar 11+6 Map V. Heavy Mineral Assemblages El Morro to Solana . . . 11+7 Map VI. Heavy Mineral Assemblages Solana to Mexico .... • • l*+8 iii LIST OF TABLES Table Page 1. Hydraulic Equivalents of Wentworth Scale for Density 3.95.............................. 10 2. Hydraulic Equivalents of Wentworth Scale for Magnetite............................... 17 3. Computed Hydraulic Equivalents Compared with Measured O n e s ........................... 18 If. Principal Source Rocks in the Tectonic Provinces of southern California......... 30 5. Average Heavy Mineral Frequencies Arranged According to Geologic A g e ................ 7*f 6. Detrital Mineral Suites Characteristic of Source Rock Types........................ 88 7. Identification of Opaque Minerals.......... 10*f 8. Identification of Pyroxenes and Amphiboles . . 105 9. Identification of Sphene and Other Titanium Oxides................................... Ill 10. Identification of Staurolites ........ 112 iv LIST OF FIGURES Figure Page 1. Index Chart Showing the State of California . . 5 2. Relationship of Grain Diameter to Settling, Threshold, and Roughness Velocities ........ 12 3. Hydraulic Diameter Equivalents .............. 15 b. Curves Showing the Probable Error in Two Frequencies of a Mineral Species ...... 25 5. Chart Showing the Major Geographic Features and Tectonic Provinces of southern California 29 6. Average Heavy Mineral Frequencies in Percent in Province I ................................b2 7. Average Heavy Mineral Frequencies in Percent in Province I I ........................... b$ 8. Average Heavy Mineral Frequencies in Percent in Province III..............................k-9 9. Average Heavy Mineral Frequencies in Percent in Province I V ..............................53 10. Average Heavy Mineral Frequencies in Percent for southern California Sediments and for the Four Heavy Mineral Provinces............ 55 11. Average Heavy Mineral Frequencies in Percent Multiplied by the Ratio...................... 58 12. Average Heavy Mineral Frequencies in Percent in Rock Outcrops and Rivers of southern California..................................60 13. Average Heavy Mineral Frequencies in Percent in Beaches of southern California............ 62 l*f. Average Heavy Mineral Frequencies in Percent in the Inshore Area Down to 50 Fathoms in southern California......... 6*f Figure Page 15c Average Heavy Mineral Frequencies in Percent in the Offshore Area beyond the 50 Fathoms Contour in southern California ............ 66 16. Percent Heavy Minerals in Beach Sands of southern California........................ 70 17* Cumulative Heavy Mineral Frequencies Along a Middle to Upper Miocene Section. Elysian Park, Eastern Santa Monica Mountains .... 76 18. Cumulative Heavy Mineral Frequencies Along a Paleocene to Middle Miocene Section. Topanga Canyon, Western Santa Monica Mountains ... 78 19. Cumulative Heavy Mineral Frequencies Along a Cretaceous to Pleistocene Section, San Clemente............................. 81 20. Cumulative Heavy Mineral Frequencies Along an Upper Chico Section, Point Loma . . . 7 . . 83 vi INTRODUCTION Reports of heavy mineral analyses of sediments were remarkably abundant in geologic publications at the begin ning of the century (Boswell, 1933)* They were introduced into the petroleum industry shortly after World War I in an effort to obtain more precise stratigraphic correla tions in surface and subsurface investigations (Kaufmann, 1950). With the tremendous expansion of micropaleontology and the development of very sensitive electric logging tools, heavy mineral studies came to be considered less convenient and less dependable than the other methods of correlation. Heavy minerals cannot be treated like electric logs because different mineral species may give similar electric impulses on the register, nor like remains of living organ isms because the minerals never lived, evolved, or had any desire or preference of environment. Heavy mineral studies must be founded on heavy mineral history, which involves source rock, erosion, deposition, time, and stability. Fox these reasons heavy minerals have not been used to any extent for correlation work in southern California; instead they have served as tools for solving only a few local problems• 1 Handin (1951) studied the petrography and physiog raphy of beach and stream sands along the southern California coast from Point Conception to Point Fermin (Map III; IV, pp. l*+5, l*f6). He concluded that streams are the principal source of beach-building sediment, that longshore currents carry sediments to great distances along the coast, and that there is a considerable offshore loss of sediment through submarine canyons. Trask (1952, 1955) studied the heavy minerals in the beaches, rivers, and offshore sands along the California coast between Monterey and Santa Barbara. He divided the area into heavy mineral provinces and concluded that most of the sand is. of local origin, but that apprecia ble parts of the sand are transported for a considerable distance along the California coast and around Point Conception and Point Dume. Emery (i960, pp. 187-190) showed the distribution of the chief heavy minerals along the coast of southern California, and divided the beaches into three heavy mineral regions: epidote between Point Conception and Ventura, augite between Ventura and Santa Monica, and hornblende between Santa Monica and Mexico. These conclu sions, which were based on a few local studies, initiated the present studies of the mineralogy of all of southern California beaches and the offshore area. In the present study the southern California region (Pig. 1) was studied for its heavy minerals. Individual mineral samples from this region were first examined and grouped into heavy mineral provinces, noting the key mineral species in each province. Second, trends of these minerals within the provinces were examined, and similari ties or deviations from these trends were noted. A neces sity for a preliminary regional study is taken for granted in all conventional stratigraphic techniques in spite of its being time-consuming, and the heavy mineral technique is no exception. The reward comes in the second stage when local samples are examined, identified and interpreted rapidly and with confidence. Acknowledgment Appreciation is extended to Drs. K. 0. Emery, T. Clements, R. H. Merriam, 0. L. Bandy, and J. W. Reith, under whose supervision this work was done, for many help ful suggestions and for guidance in this work. The author is also thankful to Mr. R. D. Terry for collecting some of the beach samples, and to Mr. R. Anderson, Mr. A. Ball, and Mr. H. Pohn for collecting some of the outcrop samples. Fig. 1.— Index chart showing the State of California. The studied area, from Point Conception to the Mexican border, is blocked. 5 100 MILE METHOD OF STUDY Selections of Suitable Grain Size Two aspects should he considered when one selects a particular grain size for heavy mineral analyses. First, which of the size fractions contains an assemblage representative of the entire sample5 second, what is the most rapid procedure that can be employed in isolating the selected grain size without sacrificing critical accuracy? The petrographic microscope puts upper and lower limits on the possible grain sizes complying with these two requirements. Grains coarses than one milli meter are mostly opaque and must be ground thinner if they are to be analyzed, and grains finer than 62 microns are identified with decreasing accuracy and speed as their diameters approach the resolving limits of the microscope. The problem of selecting a size fraction has been fully, discussed by Van Andel (1950, pp. 27, 28). His cum ulative percentage diagrams of the heavy mineral fractions of some Rhine River sands show large differences in com position between the grades. The following study of the mode of transportation of sediments from source to place of burial shows that the differences observed by Van Andel 6 ...................... " ‘ ... 7; are of general character and should be expected wherever sediments are transported. A sand grain can be moved by rolling, saltation, and suspension. Bagnold (19^2) showed that motion of a grain is initiated by rolling at an increasing velocity until the grain is lifted into saltation. As the velocity increases, a second critical point is reached at which the grain remains in suspension. A diagram, prepared by Inman (19**9) shows the relationships of the diameter of an average grain (specific gravity 2.65) to the velocity at which physical erosion begins. It can be predicted from this diagram at what threshold velocity a grain starts moving by traction. The higher the velocity, the coarser is the sand grain that can be moved. As the grains begin to advance by saltation, the finer and lighter ones have longer Jumps, whereas the coarser and heavier ones lag behind. Then, if the velocity continues to increase, each size fraction successively reaches the suspension stage (velocity higher than its settling velocity). It is seen that the grains are sorted by selection at both traction and suspension stages, and that the degree of sorting depends on the velocity of the fluid and on the size of the grains. Sand grains composed of heavy minerals are influenced by the same factors and in addition by the density of the grains, the effect of which can be seen from the Impact Formula (Rubey, 1933, 8 p. 327), V = j>-?3xgxrx (/^ - />2) - ^2]^ where: V = settling velocity of a sphere, in cm/sec g = acceleration due to gravity, 980 cm/sec x sec r = radius of the sphere, 0.0031 to 5 cm P 1 = density of the sphere (Rubey denoted this by the letter /V ) p 2 = density of the fluid (Rubey denoted this by the letter />L ) or, when considering spheres of identical diameter but different densities, V = C [(/>! ~ P2) * /£ > 23^» where: C is a constant and equals to (b - 3 x g x r)^ It can be seen that denser grains settle before lighter ones of an equivalent diameter. Taking the average density of the light minerals (lighter than 2.96) as 2.65 (which is the density of quartz), and the average density of the dominant heavy minerals of southern California as 3.95j it is possible to compute the ratio of the diameters of two spheres which settle together, but are of the two different densities. These two spheres are hydraulic equivalents of each other, and so are their diameters. This can be written as follows: V = [>*r3xgxrx (2.65 “ 1)]^ = [ ^ 3 x g x R x (3.95 “ 1)]* where: V = settling velocity of a sphere (Impact Formula), also of Its Hydraulic equivalent r = radius of a sphere having a density of 2.65 R » radius of a sphere having a density of 3*95 Solving for R, the formula can be re-written as follows: 9i H = (2.65-1) r (3.95-1* = 0.559r or, when expressed in terms of the diameters: D = 0.559cl where D = R x 2, and d = r x 2 Using this formula, the Wentworth Scale (1922) for sand grains can be converted into its hydraulic equivalent in the average heavy minerals of southern California (Table 1). Inman*s diagram (19^9) can also be modified to show the effective diameters of the hydraulic equivalents having a density of 3*95 (Fig. 2). This modified diagram illus trates the fact that although the heavy mineral hydraulic equivalents have diameters smaller by Mf.l percent than those of the average minerals, they follow the same pattern The area of traction is above the roughness velocity line, between the belt of threshold velocities and the settling velocity curve, and the area of suspension, is above all three velocities. It can be seen that a rise in velocity from 0.033 miles/hour to 0.050 miles/hour will result in an increase in the diameters of the heavy mineral grains in traction from 220 microns to 670 microns. A further rise to 0.080 miles/hour will increase the grain-size to 710 microns. A similar rise from 0.060 mile/hour to 0.080 mile/hour will increase the grain-size of the suspended heavy mineral grains from 120 microns to 150 microns. Velocities of lA to 7.2 miles/hour were measured 1 0 ! TABLE 1.— Hydraulic equivalents of Wentworth scale for density 9? NAME OF GRAIN WENTWORTH SCALE in mm. HYDRAULIC EQUIVALENT in mm. (for density 3*95) Granule J+.ooo 2.236 Very coarse sand 2.000 1.118 Coarse sand 1.000 .559 Medium sand .500 .280 Fine sand .250 .1*4-0 Very fine sand .125 .070 .062 .035 Fig. 2.— Relationship of grain diameter to settling, threshold, and roughness velocities (modified after Inman, 19^-9). Sediment of average density, 2.65. mmm— Heavy minerals of average density, 3-95« Theoretical threshold velocity, which does not apply in nature because it is below the roughness velocity. Settling velocity = [C d {p - 1)]^ (Impact Formula) Threshold velocity = 1c d (/»- 1) Roughness velocity = K/d d = Diameter of the grain P - Density of the grain C = 8/3 gravity k = Packing coefficient x Angle of repose of the grain x Roughness velocity ? Viscosity K = 3*5 x Viscosity M ILE S P E R HOUR 12 SUSPENSION, \T POSITION A ii 1 i . 1 I DIAMETER mm C m / Sec by the author during storm periods in the major rivers of the Los Angeles County, and an average velocity of about 10 cm/sec (0.22*f miles/hour) was reported by Emery (i960, pp. 115-116), for longshore surface currents. Velocities of longshore subsurface currents were reported to be half or more of those of surface ones. Thus, the range of velocities controlling the sorting of heavy minerals, dis cussed above, is within the possible limits. This should serve to indicate that the total heavy minerals supplied by the rivers to the sea are not concentrated in one preferred size fraction, but rather are distributed irregularly through the sediment, although the original size of the heavy mineral grains weathered from source rock is mostly finer than that of the light minerals, as noted by many authors. Any individual mineral species, however, having grains of approximately the same diameter, could be concen trated in a single size fraction as is shown in Figure 3* The same holds true for heavy minerals on the beach under the influence of breakers, or offshore under the influence of longshore currents, the control being the diameter and the density of the grains. It became obvious in this study that an analysis of one preferred grade might not give a representative picture of the entire sample, hence, the widest grain-size range practical within the limitations of the petrographic Fig. 3.— Hydraulic diameter equivalents, connected with light lines. Density of minerals shown by heavy lines. Bi Biotite CH Chlorite Ap Apatite Bp Epidote Op Opaque minerals ilmenlte) IL Ilmenite HA Magnetite AM Amphibole PX Pyroxene SP Sphene GA Garnet ST Stanolite TO Topaz QTZ Quartz ATB Acetylene tetrabromide DIAMETER 15 QTZ ATB 000 5 0 0 4 0 0 3 0 0 2 5 0 200 100 6 2 5 0 4 0 4 D EN SITY CH MA PX SP 6A ST TO microscope was used, that is 62 microns to one millimeter. Taking beach sands as a standard for comparing all the samples, the outcrop, river, and offshore samples were reduced to sand. This artificial sorting was done on the basis of the grain diameters, whereas in nature the beach sediments are sorted on the basis of the hydraulic effect of water on the mass and shape of the grain. Figure 3 shows the relationship between the diameter and the mass (density) of the grains. As the density of the grain goes up, its hydraulic diameter-equivalent goes down. A change in density from 2.65 (quartz) to 5*0 (magnetite) results in considerable changes in the hydraulic diameter-equivalents (Table 2). The values for magnetite, which were computed from the Impact Formula, were checked against measured values obtained by first sieving magnetite grains of a predeter mined density (5.0) through 125, 250, and 500 micron Taylor screens, to determine the diameters of the grains, then settling each fraction in an Emery Tube, to determine the diameters of their quartz hydraulic equivalents. The measured values are practically identical with the computed ones (Table 3). This means that any screen passed magne tite grains 58.7 percent coarser in diameter than would be normally selected by natural sorting on the beach. The coarsest screen used enriched the sample in magnetite, 17 TABLE 2.—- Hydraulic equivalents of Wentwpj-fe^-Sc^ig_J f . Q r . jnagnaSUa. Wentworth Scale Diameters in microns QUARTZ Impact Formula Diameters in microns MAGNETITE Change in microns 62 26 36 12? 52 73 250 10*+ 1^3 500 207 293 1000 ^13 587 Diameter of magnetite = (1.65A.0) x diameter of quartz = Al3 x diameter of quartz 18 TABLE 3.— Computed hydraulic equivalents compared with measured ones Taylor Screen Openings in / a. * Emery Tube Diamete Time in Density of Density of (25.5 °C) p in/t sec Quartz 2.65 Magnetite 5.0 Impact Formula Diameter in / a. **Wentworth Scale Quartz Grains. Equivalents of magnetite Equivalents of magnetite sec sec A*. 12? 86 135 30 300 303 250 32 260 16 610 605 500 18 510 9 1000 1210 *Emery (1938). **Wentworth (1922). . . . 19 whereas the finest screen depleted it. The relative impor tance of the enrichment or depletion, depended on the availability of diameters slightly finer than the top or lower screens. Or, when other samples containing more than one mineral species were sieved any particular species could be enriched through the upper screen, and another species be depleted through the lower one. This marginal effect would be most noticeable when the openings of the two screens were nearest to each other in diameter. For instance, if only the very fine sand (62 - 125 microns) were used for analysis, the whole range (62 - 125 microns) would have been changed. But when very fine to coarse sand (62 - 1000 microns) was used, 28 percent of the range (150 - ^13 microns) was left unchanged. Obviously the wider diameter range gives more diagnostic results. Preparation of the Samples Four different types of samples were collected for this study, each requiring a different technique of prepara tion for petrographic analysis: beach sands, river deposits, recent marine sediments, and sedimentary rocks. Beach sands are naturally nearly restricted to the desired range of grain sizes (62 microns to 1 mm), hence no preliminary preparation was necessary. Twenty grams of sand was scraped from a surface layer of each beach and a 20 split of each sample used for analysis. In the rivers and creeks about 500 grams of sample were taken from the sur face layer at each station. Each sample was then wet- sieved to eliminate sizes coarser than 1 mm and sizes finer than 62 micrcnsj the desired fraction was then split for analysis. The sea bottom samples were collected aboard R/V Velero IV, Marine Laboratory of Allen Hancock Founda tion, University of Southern California. Only the fraction finer than 62 microns was eliminated from each sample, and a split of the sand fraction was used for analysis. Sam ples from rock outcrops were first disaggregated by alter nately soaking with kerosene and water and drying (Layne, 1950). If disaggregation was incomplete, the rock was covered with water, gently pounded, and sieved after every two or three poundings. Studies by Pohn (I960) indicated that such mechanical disaggregation of a sedimentary rock is just as effective as the kerosene method. All the samples were weighed and treated with dilute hydrochloric acid (about 2 normal) which removed the car bonates and the iron oxide coating. Heavy minerals in the residue were concentrated by sedimentation in acetylene tetrabromide (specific gravity 2.96) and mounted in aroclor (index of refraction 1.66-1.67) on glass slides for a petrographic analysis. 21 Mounting of Grains for Petrographic Analysis Mounting loose grains on a slide may be a time- consuming process, and improper mounting may cause diffi culty in identification. This problem has been discussed by many authors and partial descriptions of the technique of mounting are found in many sedimentary textbooks. The following is a complete step-by-step procedures 1. Etch the number of the sample on a glass slide with a diamond pencil. 2. Dip a glass rod in water and use it to moisten a small area on the slide. 3. Place a split of the heavy mineral concentrate in the center of the moistened area. b, Pick up a drop of water on the tip of the glass rod and touch it gently to the mineral grains. The drop will spread over the moistened area and will distribute the grains evenly. 5. Put the slide over a hot plate and let the water evaporate. The mineral grains will stick to the glass. 6. Put a piece of aroclor on the mineral grains, it will melt in a few seconds without boiling. If it boils, the plate is too hot and the tem perature should be reduced. 7. Put the slide on a glass plate and let cool for one minute. 8. Press one edge of a cover glass into the aroclor so that it leans over the mineral grains. It will stick to the almost hardened aroclor and stay in position. 9. Put the slide back on the hot plate. The cover glass will slowly fall down and cover the mineral grains. Wait until the aroclor spreads under the entire cover glass. 22 10. Return the slide to the glass plate and let cool for a few minutes. The slide is ready for microscopic examination. Five samples can easily be handled concurrently, and the entire procedure should not take more than thirty minutes per round of five. Counting the Grains and Accuracy A split of the heavy mineral concentrate, when mounted on a glass slide, is not ready yet for counting. One must decide first how far to go in subdividing the mineral groups, and second, how many grains to count. A detailed examination of the heavy mineral suites in ten widely spread beach stations revealed that four mineral species or groups dominate the region: epidote, opaque minerals (magnetite and ilmenite), amphibole, and pyroxene. Eight other mineral species were found to be present in varying amounts: biotite, chlorite, garnet, zircon, topaz, apatite, sphene (including rutile, anatase, and brookite), and staurolite (including kyanite, andalu- site, and sillimanite). Some of these mineral species could be divided into subspecies, but the probable error in the frequency count of these subdivisions would be much larger than that of the combined species. The probable error also determines the minimum num ber of grains that should be counted on each slide in order 23 to get the representative frequency distribution of the mineral species. Dryden (1931) derived a formula for com puting the probable error where just a fraction of the heavy residue had been mounted and only a part of the material mounted had been counted: P.E. (in no. of grains) = 0.671 +5[(n x f x (1 - f)]^ where P.E. = probable error n = total number of grains counted on a slide f = probability (Dryden denoted this by the letter p) or, frequency in percent of a given species 1 - f= the chance that a grain will not belong to a certain species In order to express the probable error in percent of the total number of grains counted, the above function was multiplied, in the present work, by lOOf f a to give: P.E. (in % of total grains counted) = (6?.k-5f * a) (n x f x (1 - f)2 where the new symbol is a = number of grains counted of a certain species. This function is graphically summarized in Figure M-. Here the relationship of the total number of grains counted is shown for two extreme frequencies, 5 percent and 80 percent. This figure shows that when only one hundred grains were counted (which is the minimum number considered for any statistical work) the probable error is less than 3 percent of the total number counted. Another type of error which might be involved in this study is local variation in the heavy mineral com position. It can not be computed mathematically, but, Fig. — Curves showing the probable error (P.E.) in two frequencies of a mineral species expressed in percent of the total number of mineral grains counted ogi a slide. The left curve is for a low frequency (5$) j and the right one is for a high one (80^). CM TOTAL GRAINS COUNTED O when a large number of samples had been analyzed and a trend of the minerals was established, the trend was used as a guide for accuracy. A large deviation from the trend is not an error in the strict sense, but it should be investigated as such when the general distribution and behavior of the heavy minerals is sought. Actual counting of the minerals was done as follows: an entire microscopic field was inspected and the frequen cies were counted one species at a time. Then the total number of grains was counted. The total number was usually slightly larger than the sum of all the frequencies due to a number of rock fragments and altered grains. If one field did not contain at least 100 grains, more fields were counted in the same manner. This method of counting is very rapid and it gives the finest grains as much chance to be counted as the coarsest ones. It also takes all the grains into the frequency computation, even the doubtful and unidentified ones. GEOLOGY OF THE SOURCE AREAS Tectonic Provinces Four of the six tectonic provinces of California, described by Reed and Hollister (1936, p. 3)> are partly or wholly in southern California (Fig. J>)» The principal source rocks underlying these provinces are shown in Table Santa Ynez Mountains The Santa Yhez Mountains extend eastward from Point Arguello to Ventura River, and form the most westerly part of the Transverse Ranges of southern California. They consist of sedimentary rocks that are Cretaceous to Quater nary in age, but mainly of Eocene, Oligocene, Miocene, and Pliocene series. Basement rocks are exposed only in a few small areas. They consist of slightly metamorphosed arkosic sandstones, slates, and cherts that have been invaded by masses of serpentine and other basic intrusives (Bailey and Jahns, 195*0. These rocks are a part of the Franciscan group and probably are of Cretaceous age. Ventura Basin Ventura Basin lies between Santa Ynez Mountains on the north and Santa Monica Mountains on the south. It 27 Fig. 5«--Figure showing the major geographic features and tectonic provinces of southern California ***** Border of tectonic province 1. Santa Ynez Mountains 2. Santa Monica Mountains 3. San Gabriel Mountains Santa Ana Mountains 5. Palos Verdes Hills 6. Ventura River 7. Los Angeles River 8. Point Arguello 9. Point Dume 10. Point Loma 11. Ventura Basin 12. West Los Angeles Basin (Torrance Plain) 13. East Los Angeles Basin (DownerPlain) 1*+. Northern Islands (San Miguel, Santa Rosa, Santa Cruz, Anacapa) 15. Southern Islands (San Nicolas, Santa Barbara, San Clemente, Santa Catalina) 16. . Southern California Batholith A. Central Franciscan Province B. Anacapia Province C. Southern Franciscan Province D. Mohavia Province 30 TABLE M-.—-Principal source rocks in the tectonic provinces of southern California ( t ARM TECTONIC PROVINCES PRINCIPAL SOURCE ROCKS Santa Ynez Mountains Ventura Basin Central Franciscan Sedimentary Metamorphic Igneous Santa Monica Mountains Northern Islands Anacapia Metamorphic Volcanic Igneous (granite) West Los Angeles Basin Southern Franciscan Metamorphic Sedimentary Southern Islands Metamorphic Volcanic Sedimentary East Los Angeles Basin Southern California Batholith Mohavia Igneous (mainly granite, some gabbroic) ' ... ... .... . .311 j contains several intra-basin chains of hills and mountains» among which are Sulphur Mountain, South Mountain, and Oak Ridge. This basin possesses one of the thickest Tertiary- sedimentary sections in North America. The formations are well exposed, and a thickness of more than lf0,000 feet of sediments, Eocene to Pleistocene, can be measured in single sections (Reed, 1933* p. 10). Stratigraphically, these rocks are a lateral extension of the Tertiary sediments of Santa Ynez Mountains. Basement rocks are exposed in the Topatopa Mountains (not shown in the map) immediately north of Ventura Basin. These are granodiorites and related plu- tonic rocks of -Jurassic or Cretaceous age (Bailey and Jahns, 195*0. ' Santa Monica Mountains The Santa Monica Mountains form a range that extends from Los Angeles River to Calleguas Creek*where it plunges under the Pacific Ocean. It is composed mainly of Creta ceous, Eocene, Oligocene and Miocene sediments that have been derived from crystalline basement rocks, and of Miocene basaltic and andesitic volcanic flows (Durrell, 1951 ** map sheet no. 8). Westward from Point Dume the Miocene rocks contain fragments similar to the Franciscan schist. Dikes and sills which cut Middle Miocene rocks are mostly diabases, and are highly altered wherever exposed in out crops (Azmon, 1956). The core of the Santa Monica 32 Mountains comprises the metamorphic Santa Monica Slate of Triassic (?) age (Hoots, 1931, p. 90), which grades in places into mica and chlorite schists (Bailey and Jahns, 195*+> p. 81), and numerous intrusive masses of granite and granodiorite of Jurassic (?) age (Durrell, 195*f, map sheet no. 8). Los Angeles Basin Los Angeles Basin lies between Santa Monica and San Gabriel Mountains on the north, Santa Ana Mountains on the east, and Palos Verdes Hills and the Pacific Ocean on the southwest. The basement rock in this area (Woodford, et al.. 1951 * - ) is divided into two groups. First, the West ern Bedrock Complex, also called the Catalina Schist, crops out in the Palos Verdes Hills. It is composed chiefly of chlorite schists most of which are metasediments and meta tuffs. Glaueophane, actinolite, and epidote are widespread in this complex. The second group, the Eastern Bedrock Complex, northern and eastern sides of Los Angeles Basin, consists chiefly of plutonie and metamorphic rocks, most of which are Mesozoic in age. San Gabriel Mountains form the northern end of this complex with granodiorite and anortho- site as the most abundant rocks and hornblende-diorite- gneiss and quartz-pyroxene-hornblende-porphyrite dikes third and fourth in abundance (Strong and Arnold, 1905). Santa Ana Mountains form the eastern end of this complex with a core 33 of low grade metamorphic rocks overlain by slightly meta morphosed volcanic rocks, andesitic and quartz latitic in composition. All this is intruded by a great mass of j gabbro, hornblende-quartz-diorite, biotite-quartz-diorite, and granodiorite. Sedimentary rocks, Cretaceous to Pleis tocene in age, which fill up the basin, were derived from both the above basement complexes (Conrey, 1959). Southern California Batholith The southern California batholith underlies an area of more than **0,000 square miles extending from the vicinity of Riverside, southward to the southern tip of Baja California (Larsen, 195*0 • It is a great composite of late Mesozoic plutonic rocks composed of 7 percent gabbro, 91 percent tonalite and granodiorite, and 2 percent granite, and associated metamorphic rocks (Larsen, 19**8). Continental Borderland The geology of the offshore (Emery, 195**; Emery, i960, pp. 62 to 76), is similar to and as variable as that on the mainland. Rocks on the topographic highs range from Jurassic to Pleistocene in age. The most common basement rock is Franciscan-like schist that occurs on several of the islands and banks. Granitic basement rocks are known only on one northern island (Santa Cruz). Miocene 3*+ volcanics occur on nearly all islands. They are mostly andesitic, but also basaltic, dacitic, or rhyolitic in composition (Shelton, 195*0* The four northern islands, San Miguel, Santa Rosa, Santa Cruz, and Anacapa, are in line with the Santa Monica Mountains and are a continuation of the Transverse Ranges. San Miguel Island consists of Eocene and Miocene sediments, a large cover of sand dunes, and minor flows of basalt and andesite (Bremner, 1933)* Santa Rosa Island has a thick section of Tertiary rocks ranging in age from Eocene to Late Miocene (Reed, 1933) and a number of small basaltic intrusions (Kew, 1927)* Santa Cruz Island, the largest of all, is the only one of the four having exposed granitic basement. It is overlain by Franciscan-like schist, Eocene and Miocene sediments, and most abundantly, by rhyolitic, basaltic, and andesitic volcanic flows (Bremner, 1932). Anacapa Island, the smallest of the four, consists chiefly of Miocene andesitic volcanic rocks interbedded with sedi ments closely similar to the San Onofre Breccia (Scholl, 1959)• It can be seen that the islands differ from Santa Monica Mountains in not having numerous intrusive masses of granite and granodiorite, and not having anything like the Santa Monica slate. Farther south, Santa Barbara Island consists of Miocene volcanic rocks interbedded with calcareous silt, 35 and San Nicolas Island consists of Eocene sediments rimmed by Quaternary terrace deposits (Reed, 1933)* Santa Catalina Island is underlain by Franciscan schists, andesitic flows, and intrusives of the southern California batholith (Jahns, 195^> plate no. 3)> and San Clemente Island consists mostly of Miocene volcanic flows, with a few small areas of Miocene sediments and with coastal dunes in the northern half of the island. Provenance of Heavy Minerals Each of the above source rock areas includes several rock types in different proportions, hence their heavy mineral content should vary in relative abundance much more than in mineral species. The northernmost area consists almost entirely of sedimentary rocks of the Santa Ynez Mountains with very few small exposures of low grade meta sediments and basic intrusives. It should carry zircon, and garnet, epidote, and sphene. A sedimentary-metamorphic association continues through Ventura Basin and Santa Monica Mountains, but the mineral balance of these areas is offset by the introduction of intermediate igneous rocks (granodiorites) containing amphibole, and to a lesser extent, pyroxene. Sphene, zircon, and garnet should be less common in these areas leaving as common minerals epidote, amphibole, and some pyroxene. Farther south, in Los Angeles Basin, low grade metasediments and sedimentary rocks derived from them are associated with intermediate and basic (gabbros) igneous rocks, all together should be common in epidote, amphibole, and pyroxene. The southern most area is dominated by intermediate igneous rocks with some basic igneous rocks of the southern California batho lith, and it should contain amphibole, pyroxene, and biotite. DISTRIBUTION AND PROVENANCE Heavy Mineral Provinces The heavy mineral frequency by number of grains in 286 samples from rock outcrops, rivers, beaches, inshore (down to 50 fathoms), and offshore (past 50 fathoms) of southern California averages 2.7 percent of the sand. Only four mineral groups comprise 67 percent of the total heavy mineralss epidote 21, opaque minerals 25, amphibole 15? and pyroxene 6. On the basis of these four groups, southern California can be divided into four heavy mineral provinces (Map I, p. 1^35 detail see Maps II through VI, pp. Iitif-lif8): I. Epidote and Opaque minerals (magnetite and ilmenite) II. Epidote, Opaque minerals, and Amphibole III. Epidote, Opaque minerals, Amphibole, and Pyroxene IV. Amphibole and Pyroxene Province I The mainland portion of province I comprises the area downslope from Santa Ynez Mountains, extending from Point Conception on the west to Ventura River on the east. 37 The offshore portion includes all the northern and western islands, most of the Santa Rosa-Cortes Ridge, and most of the western basins (Map I, p. 1^3). This province is characterized by a dominance of epidote and opaque minerals in the heavy fraction of the sediments, hence it may be referred to as the epidote- opaque province. Slight and irregular changes in the frequencies of these two minerals were observed along the strand line (Maps II, III, pp. lM+, 1^-5), but these are not enough to prove a longshore movement of beach sands between Point Conception and Ventura River. This does not neces sarily mean that sands do not move along the coast, but rather that new sands added from land leave a greater impression on the beaches than does sand from longshore drift. At right angles to the strand line, however, a definite trend was observed. First, the river samples are dominated by the same assemblages that dominate the beaches. Second, there is a general decrease in the fre quency of epidote and opaque minerals from the rivers past the beaches down to 50 fathoms (Gaviota and San Roque Creeks, Map II). Trask (1952) described an augite province immedi ately north of Surf (Map II), with up to 55 percent augite. He showed that the mineral augite is present in appreciable but constantly diminishing amounts from its source near Morro Bay southward for more than 100 miles to Santa Barbara. He also indicated that the streams south of Avila (Avila is about M) miles north up the coast from Surf) carry little or no augite. Hence, he concluded that the source of augite is north of Avila, that a significant pro portion of the sand at Santa Barbara comes from a distance of more than 100 miles up the coast, and that this sand moves around Point Arguello and Point Conception. It must be noted here that Trask (1952) analyzed only the very fine sand fraction (62 to 125 microns), except that where the samples were so coarse that insufficient material of this size fraction was available the mineral determination was made on the next larger fraction, 125 to 177 microns. This procedure tended to concentrate the pyroxene grains which are generally of smaller diameter than most of the epidote and opaque minerals observed in this province. Even with this concentration of augite, the frequency of augite drops from the north side of Point Conception (Sample T71*+) to the south side (Sample T713)> and more still to Whale Beach, three miles down the coast (Sample T715), from 11 percent to 7 percent to k- percent, respectively (Appendix C, p. 131) . The barrier effect of the Point on the sand is obvious. In the present work only insignificant amounts of pyroxene were found in province I (Map II, p. lMf), in spite of the southward flowing longshore currents. Also, the average _ ifo heavy mineral composition of the beaches and sea floor (Fig. 6) shows a striking similarity to that of the rivers and outcrops immediately above them. This evidence definitely suggests that the main source of sediment is upstream, and, once more, that Point Arguello and Point Conception form at least a partial barrier in the path of the sand coming from the north. On the Continental Borderland, the samples from Santa Barbara and Santa Cruz basins have more than 50 per cent opaque minerals (Map I, p. 1^3), but this is mostly authigenic pyrite including a few completely pyritized foraminiferal tests. Otherwise, the epidote-opaque fre quencies are irregular and seem to be related to local outcrops on the islands and banks as well as to the regional source rock. Sand occurs in widespread layers on the floors of the basins (Emery, i960). Although the general currents, of as much as 0.5 mph, are capable of transporting some sand, most of it is believed to have been carried and deposited by turbidity currents. Province II The land portion of province II covers the area downslope from the Santa Monica Mountains, and downslope from a number of smaller mountains, Oak Ridge, and Simi Hills. It is bordered on the west by Ventura River which drains sediments from both the first and second provinces, Pig. 6.---Average heavy mineral frequencies percent in province I RIV and RX = River and rocks FMS = Depth in fathoms of offshore samples BEACH ZIRCON GARNET BIOTITE OPAQUE EPIDOTE TOPAZ SPHENE PYROXENE OLIVINE " ^3 and on the east by Los Angeles River (Maps III, IV, pp. 1*4-5 and 1^6). The offshore portion includes part of Catalina Island and Santa Rosa-Cortes Ridge, most of the southern basins, and the continental slope immediately below the described area (Map I, p. l*+3). This province is characterized by a dominance of three mineral groups: epidote, opaque minerals, and amphibole. The first two are just as prominent here as they are in the first province, whereas amphibole is just beginning to rise (Map IV). It might erroneously appear as if the first two minerals were carried in from the northern province to be joined with amphibole, the local mineral. Actually, three submarine canyons, Hueneme, Mugu, and Dume, reduce the free movement of sand eastward (Emery, i960, pp. 27j ^6-^7> 2*4-2) and so does Point Dume. These minerals probably came from the mountains upslope and not along the coast, as is suggested also by the fact that the average heavy mineral composition of the rivers and outcrops in this province shows a frequency distribution similar to that of the beach and sea floor (Fig. 7). Samples taken at right angles to the coast do not show any clear trend in the frequency distribution of heavy minerals, probably due to mixing with short-traveled sand moving down the coast. For example, El Segundo beach (Map IV, station E7, p. 1*4-6 ) and nearby offshore station H17 have just a trace of Fig. 7.— Average heavy mineral frequencies in percent in province II. RIV and RX = Rivers and rocks FMS = Depth in fathoms of offshore samples h5 MINERAL BEACH <50 PUS!>50 FH3 GARNET BIOTITE APATITE 3TAUR0LITE CHLORITE EPIDOTE TOPAZ AMPHIBOLE PYROXENE OLIVINE Pereont he pyroxene, whereas farther offshore pyroxene goes up to 8 percent (A19), to 3 percent (B19), and to 11 percent (C19). The source of this pyroxene may be Ballona Creek, less than two miles upstream. On the Continental Borderland, Santa Monica Basin received some of its sediments from Santa Monica Bay to the north of it. However, the similarity in mineral fre quencies (particularly of epidote) in the basin to the ones on the bank south of it (stations F^-9 and G^-9, Map I, p. I*f3) shows that at least part of the sediments in the basin could have come from the south and west. The sand portion of sediment oh the sill between Santa Monica and San Pedro basins (F^7), approaches being an ore grade; 20 percent of the total sand is magnetite and ilmenite. This concentration of the iron surpasses that of Redondo Beach (C3) with its 6 percent of the total sand, but does not reach the 67 percent in the Malaga Cove sample (HA82). San Clemente Basin probably received sediments from the mainland and the islands. The other basins in this province obtained their supply of sand-size sediments from the islands and banks, and none from the mainland. Only two samples, B53 and D53, contain abundant authigenic pyrite with some completely pyritized foraminiferal tests. *7 Province III The land portion of province III covers the area downslope from San Gabriel and Santa Ana Mountains* It is bordered on the west by Los Angeles River which drains sediments from both the second and third provinces. On the east it is bordered by the western slopes of Elsinore and Santa Margarita mountains* The submarine portion includes San Pedro Basin, most of San Diego Trough, San Clemente Island, and parts of Catalina Island and Cortes Bank (Map I, p. 1**3). This province is characterized by a dominance of four mineral groups: epidote, opaque minerals, amphibole, and pyroxene. Here, too, as in province II, the heavy mineral assemblage of the beaches and offshore is prac tically identical with that of the rivers and outcrops, again showing that the former obtained their characteris tics from the latter (Fig. 8). The drainage pattern in this province clearly demonstrates how these minerals have assembled. The western tributary of Los Angeles River (Map IV, p. 1^6) drains sediments from eastern Santa Monica Mountains in province II, almost as far north as Simi Hills. Its Rio Hondo tributary drains San Gabriel Mountains in province III, and so does the San Gabriel River. Santa Ana River drains the northern portion of Santa Ana Mountains as well as San Bernardino Mountains more than 120 miles Fig. 8.— Average heavy mineral frequencies in percent in province III. RIV and RX = Rivers and rocks FMS = Depth in fathoms of offshore samples 1*9 s ill MINERAL < 50 BH3|>50 P S XVERAGS RIV&RX BEACH ZIRCON BI0TITE APATITE STAUROLITE CHLORITE EPIDOTB TOPAZ AMPHIBOLE SPHENE OLIVINE Percent 0 50 0 0 50 5o o 5o o 50 50 northeast of the coast, and San Juan Creek drains the southern portion of Santa Ana Mountains, still in province III, as well as Elsinore Mountains which are in province IK In this province, as in the former one, local mixing on the beach and near shore mars any possible directional trends. Very little sand, if any at all, can move south along the shore past Redondo Canyon (Emery, I960, p. *+7) and the cliffs of Palos Verdes Hills. This shows very well in the considerable decrease in frequency of opaque miner als going from Redondo Beach (sample C3) north of the hills, to Bluff Park (sample H13) south of them (Map IV, p. 1^-6). On the Continental Borderland, the pyroxene in San Pedro Basin (IV7) is more abundant than amphibole and may be related to the nearby Catalina Island (1^9) and not to the mainland (C22). The beach sand from San Clemente Island (Cft-5) and the sand from Cortes Bank (D51) are prob ably also related to local outcrops. Province IV The mountain ranges in province IV extend more or less parallel to the coast, with eight major rivers cutting them into segments and flowing southwest into the Pacific Ocean. Elsinore and Santa Margarita mountains border this province on the north, and Mexico borders it on the south (Maps V, VI, pages 1^7> lM-8). The submarine portion includes parts of San Diego Trough (Map I, p. 1^3). This province is characterized by a dominance of amphibole, pyroxene, and opaque minerals (Map V, p. 1^7)• Epidote is still present, but is in a considerable decline below the other provinces. Here again (Fig. 9) the average heavy mineral frequencies in the rivers and rock outcrops is close enough to those of the beach and offshore to sug gest that the main contributors to the sediments in the sea are the mountains upslope and not along the coast. Local movement of sediment parallel to the coast possibly marred any sign of trend in the movement at right angles to the coast. Little or no sediment, however, is transported across La Jolla Canyon (Emery, I960, p. *+7)* or around the cliffs of Point Loma. Coronado Bank (EM12) and Los Coronados Island (EMl^f) have only a trace of pyroxene. The position of Coronado Canyon, between the bank and the island, rules out the possibility that sand is being sup plied to the bank from the south. Trends in Averages It can be seen (Fig. lo) that the average frequen cies of epidote and opaque minerals are highest in province I and decline toward province IV, whereas those of amphi bole and pyroxene increase in the same direction. It may appear as if each successive province has some minerals carried over from the province north of it, plus a new species derived locally. But, when giving the frequencies Pig. 9.— Average heavy mineral frequencies in percent in province XV. RIV and RX = Rivers and rocks FMS s s Depth in fathoms of offshore samples 53 RXV&flX i BEACH ■< 50 F-- v>50 F. ‘ . ! AVSRA05 ZIRCON BIOTITE APATITE OPAQUE 3TAUR0LITE TOPAZ SPHENE PYROXENE Fig. 10.— Average heavy mineral frequencies in percent for southern California sediments and for the four heavy mineral provinces. 55 u IV lAVERAOS II in ZIRCON BIOTITE APATITE OPAQUE 3TAUR0LITE CHLORITE EPIDOTE TOPAZ AMPHIBOLE SPHENE PYROXENE OLIVINE % HEAVIES « ■ 10 percent ~ 56 an absolute value (to avoid the interrelation of the fre quencies which must add to 100 percent in each sample), multiplying them by the ratio of the percentage of heavy minerals in the province to the percentage of heavy miner als in province I, it is revealed (Fig. 11) that the epidote and opaque minerals do not decrease going south, but are irregular, and their frequencies in province IV are even higher than in province I. The longshore currents which may be locally influential could not carry sediments across the submarine canyons and around the points, as will be shown later. A comparison of the unweighted frequencies with those of the rivers and outcrops (Fig. 12) shows their similarity in distribution. These are igneous and conti nental sediments, both of which are beyond the reach of the longshore currents and the waves. Comparison of the unweighted average frequencies with those of the beaches (Fig. 13) shows similar relations and leads to the same conclusions. It is not surprising then that the offshore samples (Figs. I1 *, 15) > t°o, agree with the above frequency relations. In summary, each of the heavy mineral provinces cuts through a number of environments of deposition. Percentage of Heavy Minerals The ratio of the total weight of the heavy minerals Fig. 11.— Average heavy mineral frequencies in percent multiplied by the ratio: % heavy minerals in the province X % heavy minerals in province I 0.8 IV II III ZIRCON GARNET 3I0TITB APATITE SPAUROLITE CHLORITE TOPAZ AMPHIBOLE SPHENE OLIVINE 0 200 0 200 percent q 200 0 200 Fig. 12.— Average heavy mineral frequencies in percent in rock outcrops and rivers of southern California. MINERAL IX XIX AVERAGE IV ZIRCON GARNET BIOTITE APATITE OPAQUE STAUROLITE CHLORITE EPIDOTE TOPAZ AMPHIBOLE SPHENE PYROXENE OLIVINE % HEAVIES ' 10 pereent Fig. 13.— Average heavy mineral frequencies in percent in beaches of southern California 62 MINERAL II III zircoi; GARNET BIOTITE APATITE OPAQUE STAUROLITE CHLORITE EPIDOTE TOPAZ AMPHIBOLE OLIVINE 0 0 0 Peroent Fig. Ilf.— Average heavy mineral frequencies in percent in the inshore area down to 50 fathoms in southern California. 6^ * IV II ,111 ZIRCON CHLORITE EPIDOTE TOPAZ 3PHENE Fig. 15.— Average heavy mineral frequencies in percent in the offshore area beyond the 50 fathom contour in southern California. 66 XV KvwiUvGi] II GARNET BIOTITE APATITE OPAQUE STAUROLITE CHLORITE EPIDOTE TOPAZ AMPHIBOLE SPHENE PYROXENE OLIVINE poroont In a sand sample to the total weight of the sample, expressed as parts per hundred, is the percent heavy miner als or, as it is sometimes called, the hydraulic ratio of the sand. The latter term, however, implies that the hydraulic energy of the transporting waters is the ultimate factor influencing the concentration of heavy minerals. This implication ignores the primary importance of the source rock. For example, the average composition of five granodiorites (LA16) which were analyzed by Larsen (19^8) shows 9 percent heavy minerals, whereas the average of four gabbros (L&17), also analyzed by him, shows 3*+ percent heavy minerals. Just as important may be the stability of the mineral. Larsen (19^8) found in a few rocks in San Marcos Mountains (Lkb) as much as Ik- percent of olivine (of the total samples); nevertheless the present work shows that only a trace of olivine survived long enough to reach the nearest beaches. On the other hand, this work shows that topaz,* which is in the lower third of Pettijohn's (19^9) stability list, constitutes 5*5 percent of a beach sand (G7) continually exposed to the waves. This apparent sta bility of topaz might be due to a protective coating of calcium carbonate which composes more than 6o percent of this beach. A similar phenomenon was observed by Slatkin and Pomeraneblum (1958) where a calcareous coating pro tected tremolite from weathering. The importance of *Tentative, as no clear EXa figure observed. hydraulic control of the minerals is not minimized by the introduction of additional controlling factors, and it is fully discussed in the section on selection of a grain size. Finally, the concentration is influenced by diagene sis of minerals. This process reached important dimensions in four basins where authigenie pyrite comprises more than 50 percent of the heavy fraction (A*f5> B53» 053)• The average percentage of heavy minerals for the entire region is 2.7 percent. The average for province IV is 5 percent, which is the highest of all provinces, and that of province I is only 0.8 percent which is the lowest one (Fig. 16). Multiplying the frequencies of the mineral species by the corresponding percent heavy minerals gives the frequencies their proper weight. For example, zircon seems to constitute about 1 percent of the heavy minerals in the beach samples in all four provinces (Appendix D-2, page 1^0). But, adjusting for the differences in the per centage of heavy minerals of the provinces, the absolute values of the frequencies show that province II has 15 times more zircon than province I, and province IV has twice as much zircon as province II. Zircon is only an accessory constituent both in acid igneous rocks and in metamorphic rocks; thus, a difference in source rock alone is not likely to cause the above difference in frequency. Also, zircon is the most persistent heavy mineral and it is not Fig. 16.— Percent heavy minerals in heach sands of southern California. PT = point SC = Submarine canyon — — = Average of the provinces m PT.DUME — V--- PT.FERMIN —- y ---- ENEM ESC ’ REDONDO SC NEWPORT SC * UT. SVCCANVON MALIBU C. * L. A.RIVER * T F SG.RIV. S .A .R I V .T f 1--- SAN JUAN CREEK PTLOMA LAjQ LLA SC EI7 AI 7 I POINT | CONCEPTION C 3 HI3 10 S C I3 r\iTMii<T PROVINCE I 1 p r o v i n c e iv PROVINCE I I I PROVINCE I I 71 likely to be authigenic in origin. Little zircon, if any, could come from up the coast, as discussed in the section on the provinces. One is left to believe that the increase in zircon is due to a longer time of reworking which reduced the concentration of some of the other minerals. A few interesting relationships between the heavy minerals and the beaches are brought in Figure 16, which shows the percent heavy minerals along the beaches from Point Conception to the Mexican border. Three major projec tions in the coast line of southern California are marked by a considerable drop in the heavy mineral concentration: Point Dume, Point Fermin, and Point Loma. This drop may be due primarily to the nearby submarine canyons (Dume, Redondo, and La Jolla submarine canyons). A drop in the heavy mineral curve is created also by Newport canyon thus little or no sand is carried across any of the mentioned canyons (Emery, i960). Hueneme submarine canyon, too, shows a drop in the percent heavy minerals, but this effect is hardly noticeable as beaches on both sides are very low in heavy minerals. The heavy mineral concentration in the beach above Redondo canyon is one of the highest of all the beaches in southern California and, as mentioned in the seo- tion on province II, this beach contains more than 6 percenb magnetite and ilmenite. The percentage of heavy minerals is high, too, as might be expected at the outfall of the 72 following major streams: Little Sycamore and Malibu can yons , Los Angeles River, and San Juan Creek, San Gabriel and Santa Ana Rivers appear small in comparison with Los Angeles River. Several other peaks and troughs in the percent of heavy minerals curve seem to have no apparent explanation. Age and Correlation Studies of heavy minerals in ancient rocks have been carried on by a number of authors in different parts of the world. For example, Hoots (192?) found that distinct stratigraphic variations occur in the heavy mineral content of late Tertiary sediments in San Joaquin Valley, California. Feo-Codecido (1955) was able to correlate rocks, Cretaceous to Pleistocene in age, in Venezuela on the basis of 55»000 heavy mineral analyses, and Koen (1955) used heavy minerals as an aid to correlation of ancient sediments in the northern part of the Union of South Africa Each of the correlations made by the above authors seems to be between genetically related rocks, each being most probably within a single heavy mineral province. Correla tions by some other authors appear to be useless, possibly because their analyses happened to cut across more than one province. In the present study, the average heavy mineral frequencies according to age, without any consideration of the provinces (Table 5), shows no systematic trend at all. This may be due to the fact that the same source rocks sup plied sediments all through the Tertiary and are still sup plying them today. Hence any successive stage consists of reworked sediments from the preceding stage, as well as of sediments derived directly from the source. Local changes, however, in the source rock or in the direction of supply within the provinces could have resulted in differences in the mineral composition of a sediment and these changes were examined in detail. For instance, the heavy mineral samples along a Middle to Upper Miocene section, Elysian Park, Eastern Santa Monica Mountains (Fig. 17; May IV, p. l*+6), are located in the interface of the second and third provinces; hence, they may be expected to be domi nated by epidote, opaque minerals, amphibole, and a little pyroxene. The lower five stations on this section (3*+9 to C57) carry the expected mineral suite, but from there upsection (D57 to C^9) amphibole and pyroxene disappear completely. It may very well be that this change points the break between the Middle and Upper Miocene strata. In another section of heavy mineral samples (Fig. 18; Map III, p. 1^5), Paleocene to Middle Miocene in age at Topanga Canyon, Western Santa Monica Mountains, the Paleocene is dominated by opaque minerals, the Eo-Oligocene by epidote, and the Miocene by both species. The dominance TABLE 5.--Average heavy mineral frequencies arranged, according to geologic age MINERAL G E 0 L 0 G I C A G E o •H w A #»' 0 •H W m a 1 Cretaceous Paleocene Eocene Oligocene Miocene Pliocene Pleistocene i i ZIRCON 0 * P 1 1 1 3 P 3 1 GARNET 1 P P 3 1 2 2 2 1 BIOTITE 30 23 36 0 h 2 0 l*f 1 APATITE 0 p P 0 1 0 0 0 0 OPAQUE 10 16 7 83 18 21 29 b2 32 STAUROLITE 1 0 P 0 0 0 0 0 0 CHLORITE 0 6 P 0 5 1 0 2 0 EPIDOTE 10 17 6 5 ?o 50 2b 5 38 TOPAZ 0 0 0 0 l l 0 0 0 AMPHIBOLE 20 23 2b 0 b 3 6 15 6 SPHENE 1 P P p b 1 0 0 PYROXENE 0 7 18 7 P 3 10 2 3 OLIVINE 0 0 3 0 0 0 6 0 0 % HEAVIES 6.8 3.3 1.6 0.1 o.k 6.0 3.7 0.7 *p = present, less than one percent. Fig. 17.— Cumulative heavy mineral frequen cies along a Middle to Upper Miocene section, Elysian Park, eastern Santa Monica Mountains. PX = Pyroxene; AM = Amphibole The blackened and dotted patterns are used here as a visual aid and should not be confused with the symbols on the maps. 76 / MIDDLE MIOCENE UPPER MIOCENE 00 OTHER PX. 50 OPAQUE EPIDOTE B A A B C D E F C 49 5 7 49 57 57 57 57 57 4 9 Fig. 18.— Cumulative heavy mineral freauen- cies along a Paleocene (P) to Middle Miocene (MM) section, Topanga Canyon, western Santa Monica Mountains. E-0 = Eocene to Oligocene LM = Lower Miocene AM = Amphibole 78 UJ > D 2 D (J 100 OTHER AM. OPAQUE 50 EPIDOTE 0 C DEB 55 55 55 55 of epidote in the Eocene is even more prominent along a Cretaceous to Pleistocene section near San Clemente (Fig. 19; Map V, p. 1^7). In still another section (Fig. 20; Map VI, p. 1^8) Upper Chico (Late Cretaceous in age) at Point Loma, the lower Upper Chico is dominated by epidote, the middle and upper Upper Chico are dominated by amphibole, and the Pleistocene, which obviously lies unconformably on top of the upper Upper Chico, is also dominated by amphibole, and contains more of this mineral than do the underlying rocks. Fig. 19.— Cumulative heavy mineral frequen cies along a Cretaceous (K) to Pleistocene (PLS) section, San Clemente* P a- Paleocene E s t Eocene LM = Lower Miocene MM = Middle Miocene QM = Upper Miocene (Paleocene sample is 100$ hematite) 81 100 OTHER PX 50 ui OP. EPIDOTE A B C D E 45 45 47 47 47 47 4 7 Fig. 20.— Cumulative heavy mineral frequen cies along an Upper Chico section, Point Loma. L « Lower Chico M = Middle Chico U = Upper Chico PLS = Pleistocene CUMULATIVE 100 OTHER AMPH 50 OP. EPIDOTE G H I A 53 53 53 55 SUMMARY AND C O N C L U S I O N S An understanding of the laws that govern the history of a heavy mineral grain is necessary for the proper deciphering of this history. For instance, it is important to know that the total heavy mineral assemblage in nature is not concentrated in one preferred size fraction, although individual mineral species may be so concentrated. For this reason, it is advisable to use the total sand for analysis, or at least a broad range. The sand of the range from 62 microns to one millimeter is used here and found satisfactory. Sorting of heavy mineral grains in nature, like the sorting of light minerals, depends upon the velocity of the water and the size of the grains. But, the heavy minerals, being denser than the average sediment (specific gravity of 3*95 instead of 2.65)» are sorted also according to their density in such a way that heavy mineral grains of smaller diameters are carried and deposited along with light mineral grains of larger diameters. Such light and heavy mineral grains are hydraulic equivalents of each other. When any preferred size fraction is sorted out by screening in the laboratory during preparation for analysis, each screen permits the passage of heavy mineral grains 8*f _ _ 35 which are hydraulic equivalents of light mineral grains which are retained by the screen. The uppermost screen thus permits enrichment of the heavy minerals, and the lowest screen permits loss of heavy grains which should stay in. This marginal effect of the screens can be con siderably reduced by using the total sand, or rather the range 62 microns to one millimeter. The probable error due to splitting each sample a number of times before mounting, and then counting only a portion of the mounted grains, but more than 100, is less than 3 percent of the total number of grains counted on each slide. This error was taken into account by rounding the frequencies to the nearest 5 percent, on the maps. The true reliability of the counts, however, can be better evaluated by comparing each individual slide with the over all trend in the region. Four mineral species or groups dominate in the region: epidote, opaque minerals (magnetite and ilmenite), amphibole, and pyroxene. Eight other minerals are present in varying amounts: biotite, chlorite, garnet, zircon, topaz, apatite, sphene and staurolite. On the basis of the four key minerals, southern California is divided into the following heavy mineral provinces: I. Epidote and Opaque minerals (magnetite and ilmenite) II. Epidote, Opaque minerals, and Amphibole III. Epidote, Opaque minerals, Amphibole, and Pyroxene IV. Amphibole and Pyroxene A comparison of samples from rock outcrops and riv- jers, beaches, sea floor and islands, shows that the main \ control of the heavy mineral distribution is not within the environment of deposition (streams, beaches, sea floor) but rather within the heavy mineral provinces which may and do cut through a number of environments. It shows also that : the main supply of sand for the beaches and sea floor comes directly from the land above. The geology of the supposed source area confirms this conclusion and shows once more 'the relationship between the heavy mineral provinces and the source. Supply by longshore movement of sand is secondary and of only local importance, as obstacles along the coast, such as submarine canyons and points, cut the coast into many small segments having independent longshore movement of sediments. When average heavy mineral frequencies are arranged according to the geologic ages of the samples, without any consideration of the provinces from which they were taken, they show no trend at all. Local groups of samples, how ever, when arranged in order of age and compared within the province in which they were collected, do show trends. Detrital mineral suites characteristic of various types of source rock have been compiled by the author from Claris: (1959), Durrell (19^7), Milner (19*K», Pettijohn (19^9), Winchell and Winchell (1951), and Wahlstrom (19^7), ;(Table 2). A comparison of the average heavy mineral suite |of the beaches south of Santa Ynez Mountains (province I) with Table 2 suggests a combination of metamorphic source ;rock (epidote and staurolite) with acig igneous source rock; (zircon and topaz). The basement rocks in province I fall into this category. Reworking of sediments during the Tertiary apparently brought epidote and opaque minerals to their present concentration. The beach sands immediately south of Ventura Basin (province II) have heavy mineral suites dominated by epidote and opaque minerals, like the beaches up coast, except for a rise in the frequency of amphibole, which is to be expected due to the introduc tion of granodiorltes (Table 6), The beach sands south of Santa Monica Mountains, still in province II, have heavy mineral suites dominated by epidote, opaque minerals, and amphibole. These are the expected species in a sediment derived from a metamorphic-granodiorite source (Table 6). The beaches south of Los Angeles Basin (province III) have heavy mineral suites dominated by epidote, opaque minerals, amphibole, and pyroxene. This assemblage shows very clearly the effect of the Bedrock Complexes, The beaches south and west of the southern California batholith (province IV) have heavy mineral suites dominated by 88 TABLE 6.--Detrital mineral suites characteristic of source rock types I MINERAL (H S M 8 M i PEGMATITE 8 8 O H o 8 « 8 MEIAMORPHIC REWORKED SEDIMENTS OLIVINE P : EPIDOTE i P p P P C (C) : APATITE P p P P P C I GARNET P p C P P C (P) PYROXENE P p c C c P : AMPHIBOLE P c c c c P j OPAQUE c c p P c C c ; BIOTITE c c c c p c SPHENE p p p P p P p CHLORITE P p p P p p STAUROLITE c c TOPAZ c p ZIRCON c c c P p c *Compiled from Clark (1959), Durrell (19^7), Milner (19*K)), Pettijohn (19^9), Winchell and Winchell (195D, Wahls trom (19*+7). C = common (C) = common if available p = present 89 amphibole, with pyroxene second in abundance, and opaque minerals and epidote third. This is exactly the order of importance suggested by the batholithic rock associations ;(Table 6). The four northern islands (San Miguel, Santa Rosa, Santa Cruz, and Anacapa) differ from the Santa Monica Mountains in not having numerous intrusive masses of gran ite and granoaiorite, and not having anything like the Santa Monica slate. These differences were apparently enough to reduce the amphibole content on the beaches of the islands and, hence, to keep the islands within heavy mineral province I. The basic volcanic flows on Santa Cruz and Anacapa Islands could not change this picture, as only the relatively few sand size phenocrysts and none of the aphanitic groundmass could affect the composition of the beach sands. The area of schists on Catalina Island falls within the heavy mineral province III, which is dominated by epidote, opaque minerals, amphibole, and pyroxene, whereas the area of volcanic and intrusive rocks fails within province II, which is dominated by only epidote, opaque minerals, and amphibole. San Clemente Island and Cortes Bank, which consist mostly of Miocene volcanic flows, form two isolated patches of province III. i E C O N O M I C GEOLOGY Heavy mineral analyses can be used for stratigraphic correlation along with other means of correlation. How ever, the concept of time, as used for correlation, should be considered in terms of structural evolution of the source area, and not in terms of the rate of deposition, because it is the change in the source rock and in the pattern of drainage that causes a changed mineral suite at the site of deposition. Also, because highlands usually shed sediments to the seas immediately below them, a heavy mineral survey of ancient marine sediments can give a hint as to the direction of the highland, which in most cases is also the direction of the land and the direction of the strand line. Knowing this direction is of extreme impor tance in the search for stratigraphic oil traps, as this direction points to the primary high areas toward which oil could have migrated. 90 REFERENCES REFERENCES Azmon, E.. 1956, The geology of Point Mugu Quadrangle: unpublished Master’s thesis in geology, University of California at Los Angeles, 37 P- Bagnold, R. A., 19^2, The physics of blown sand and desert dunes: W. Morrow & Co., New York. Bailey, T. C. and Jahns, R. H., 195^, Geology of the Transverse Range Province, Southern California: California Div. Mines Bull. 170, p. 83-106. Bellemin, G. J. and Merriam, R., 1958* Petrology and origin of the Poway conglomerate, San Diego County, California: Geol. Soc. America Bull., v. 69, p. 199- 220. Boswell, P. G. H., 1933> Mineralogy of sedimentary rocks: T. Murby & Co., London, 395 P* Bremner, C. St. J,, 1932, Geology of Santa Cruz Island, Santa Barbara County, California: Santa Barbara Mus. Nat. Hist. Occ. Paper No. 1. , 1933, Geology of San Miguel Island, Santa Barbara County, California: Santa Barbara Mus. Nat. History Occ. Paper No. 2. Carroll, D., 1953, Weatherability of zircon: Jour. Sedi mentary Petrology, v. 23, p. 106-116. Clark, F. W., 1959, Data of geochemistry: U. S. Geol. Survey Bull. 770, 5th ed., 8*H p. Conrey, B. L., 1959, Sedimentary history of the Early Pliocene in the Los Angeles basin, California: unpub lished Ph. D. dissertation, University of Southern California. Davis, E. F., 1918, The Franciscan sandstone: University of California publication, Bull. Dept. Geol,, v. 11, p. 1-Mf. 92 93! i Dryden, A. L.. 1931, Accuracy in percentage representation of heavy mineral frequencies: Proc. Nat* Acad* Sci*, v. 17, p. 233-238. Durrell, Cordell, 19^7, Classification of the igneous rocks: Rock Chart, University of California at Los Angeles* . 195^, Geology of the Santa Monica Mountains, Los Angeles and Ventura Counties: California Div. Mines Bull* 170, Map sheet No. 8. Emery, K. 0*, 1938, Rapid method of mechanical analysis of sands: Jour. Sedimentary Petrology, v. 8, No. 3, p. 105-111. Emery, K. 0., Butcher, W. S., Gould, H. R. and Shepard, F. P., 1952, Submarine geology off San Diego, California: Jour. Geology, v. 60, No. 6, p. 511-5*+8. Emery, K. 0., 195*+* General geology of the offshore area, southern California: California Div. Mines Bull. 170, p. 107-111* * i960, The sea off southern California: John Wiley and Sons, Inc., New York, 366 p. Feo-Codeeido, G., 1955> Heavy mineral techniques and their application to Venezuelan stratigraphy: Am. Assoc. Petroleum Geologists Bull., v. 5, P* 98M—1000. Gianella, V. P., 1928. Minerals of the Sespe formation, California and their bearing on its origin: Am. Assoc. Petroleum Geologists Bull., v. 12, p. 7^7-752. Handin, John, 1951, The source, transportation, and deposi tion of beach sediments in southern California: Beach Erosion Board, Office of the Chief of Engineers, Dept, of the Army, Corp of Engineers, Technical Memorandum No. 22, 125 p. Hertlein, L. G. and Grant, IV U. S., 19^, The geology and paleontology of the marine Pliocene of San Diego, California: Mem. San Diego Soc. Nat. Hist., v. II, Part 1, 72 p. Hoots, H. W., 1927, Heavy mineral data at the southern end of San Joaquin Valley: Am. Assoc. Petroleum Geologists Bull., v. 11, p. 369-372. Hoots, H. W.. 19319 Geology of the eastern part of the Santa Monica Mountains, Los Angeles County, California: U. S. Geol. Survey Prof. Paper 165-C, p. 83-13^. Inman, D. L., 19*+9, Sorting of sediments in the light of fluid mechanics: Jour. Sedimentary Petrology, v. 19, I P. 51-70. Jahns, R. H., 195*+, Geologic map of the Transverse Range Province, southern California: California Div. Mines Bull. 170, Chapter II, Plate *+. ______ , 195*+> Geologic map of the Peninsular Range Province, southern California: California Div. Mines Bull. 170, Chapter II, Plate 3* Kaufman, G. F.. 1950, Modern methods in petroleum explora tion: Quart. Colorado School Mines, v. No. 1 B, P . 36-69. Kew, W. S. W., 1927, Geologic sketch of Santa Rosa Island, Santa Barbara, California: Geol. Soc. America Bull., v. 38, p. 6^5-65^. Koen. G. M., 1955, Heavy minerals as an aid to the correla tion of sediments of the Karroo System in the northern part of the Univ. of South Africa: unpublished Ph. D. dissertation, IJhiv. Pretoria, 213 P* Larsen, £• S., 19^8, Batholith and associated rocks of Corona, Elsinore, and San Luis Rey Quadrangles, southern California: Geol. Soc. America Bull., mem. 29, 182 p. ______ • 195^> Ike batholith of southern California: California Div. Mines Bull. 17G, Chapter VII, p. 25-30. Layne, M. M., 1950, The gasoline method for the disintegra tion of argillaceous shales: The Micropaleontologist, v. !*, No. 1, p. 21 Milner, Henry B., 19^0, Sedimentary petrography: Thomas Murby & Co., London, 666 p. Pettijohn, F. J., 19^9, Sedimentary rocks: 1st ed., Harper & Brothers, New York, 526 p. Pohn, A. H., i960, A method of disaggregating sandstones and its effect on original grain size: unpublished paper in sed. tech., sedimentation lab., University of Southern California. 95 Reed, R. D., 1933* Geology of California* Am. Assoc. Petroleum Geologists, Tulsa, Oklahoma, 355 P- ■ _ . . . and Hollister, J. S., 1936, Structural evolution of southern California: Am. Assoc. Petroleum Geologists, Tulsa, Oklahoma, 157 P« IRubey, W. W., 1933i Settling velocities of gravel, sand, j and silt particles: Am. Jour. Sci., v. 25* Wo. 1**8, P. 325-338. jScholl, David W., 1959> Geology and surrounding recent marine sediments of Anacapa Island: unpublished Master^s thesis in geology, University of Southern California, 105 P« Shelton, J. S., 195^* Miocene volcanism in coastal southern California: California Div. Mines Bull. 170, Chapter VII, p. 31-36. ■Slatkine, A. and Pomerancblum, M.. 1958, Unstable heavy minerals as criteria of depositional environment: Geol. Survey Israel Bull. No. 19, 11 p. Strong. A. M. and Arnold, R.. 1905* Some crystalline rocks of. the San Gabriel Mountains, California: Geol. Soc. i America Bull., v. 16, p. lSS-^O1 *. Trask, P. D., 1952, Source of beach sand at Santa Barbara, California as indicated by mineral grain studies: Dept, of Army, Corp of Engr., Beach Erosion Board Technical Memo # 2o, 2*f p. , 1955} Movement of sand around southern California promontories: Dept, of Army, Corps of Engineers, Beach Erosion Board, Tech. Memo 76, 6o p. Van Andel, T. H., 1950, Provenance, transport and deposi tion of Rhine sediments. A heavy mineral study on river sands from the drainage area of the Rhine Geol. Lab. of the Agricultural Univ. at Wageningen, Netherlands, 129 p. Wahlstrom. E. E., 19*+7> Igneous minerals and rocks: John Wiley & Sons, Inc., New York, London, 367 p. Wentworth, C. K., 1922. A scale of grade and class terms for clastic sedimeucs: Jour. Geol., v. 30, p. 377-392. Winchell, A. N. and Winchell, H.. 1951> Elements of optical mineralogy, part II, description of minerals: *+th ed., John Wiley & Sons, New York, 551 p. Woodford, A. W., Schoellharaer, J. E., Vedder, J. G. and Yerker, R. P., 195*+j Geology of the Los Angeles basin: California Div. Mines Bull. 170, Chapter II, p. 65-81. 96 SUPPLEMENTARY BIBLIOGRAPHY Chepil, W. S., 19*+5, Initiation of soil movements Soil Sci., v. 60, No. 6, p. 397-1 fll. Clements, T. and Dana, S. W., 191 +1 + - , Geologic significance of a coarse marine sediment from near Santa Catalina Island, California: Jour. Geol., v. 52, p. 351-35^. ! ■ Cogen, W. M.. 1935, Some suggestions for heavy mineral investigations of sediments: Jour. Sedimentary Petrol ogy, v. 5, p. 3-8. Dibblee, T. W., Jr., 1950, Geology of southwestern Santa Barbara County, California: California Div. Mines Bull. 150, 95 P. Emery, K. 0. and Shepard, F. P., 19^5, Lithology of the sea floor off southern California: Jour. Geol., v. 56, p. 1+31-^78. Hjulstrom, Filip, 1939, The transportation of detritus by moving water: Recent Marine Sediments, Am. Assoc. Petroleum Geologists Symposium, Editor P. D. Trask, p. 5-31. Holzman, J. E., 1950, Submarine geology of Cortes and Tanner Banks: unpublished Master*s thesis in geology, University of Southern California, k-7 p. Hutton. C. 0., 1952, Accessory mineral studies of some California beach sands: U. S. Atomic Energy Commission RMO-98I, 112 p. Inman, D. L., 1953, Areal and seasonal variations in beach and nearshore sediments at La Jolla, California: Dept. Army Corp Engr. Beach Erosion Board, Tech. Memo 39, 82 p. Kelley, F. R., 19^3, Eocene stratigraphy in western Santa Yhez Mountains, Santa Barbara County, California: Am. Assoc. Petroleum Geologists Bull., v. 27, p. 1-19. Kew, W. S. W., 192^, Geology and oil resources of a part of Los Angeles and Ventura Counties, California: U. S. Geol. Survey Bull. 753* 97 KrUmbein, W. C. and Pettijohn, F. J., 1938, Manual of sedimentary petrography: D. Appleton-Century Co,, Hew York, & 9 p. Larsen, E. S. and Berman, E., 1931 * - , The microscopic deter mination of non-opaque minerals: U. S. Geol. Survey Bull. 8M, 265 p. Merriam, P. 0., 19^9> Geology of the El Segundo sand hills: unpublished Master’s thesis, Uhiversity of Southern California, p, Merriam, Richard, 19^6, Igneous and metamorphic rocks of the southwestern part of the Ramona Quadrangle. San Diego County, California: Geol. Soc. America Bull., v. 57, p. 223-260. ______, 195^A typical portion of the southern California batholith, San Diego County: California Div. Mines Bull. 170, Map sheet 22. Miller, W. J., 193*N Geology of the western San Gabriel Mountains: Publications in Math, and Phys. Sci., v. 1, University of California at Los Angeles. Natland, M. L. and Kuemen, Ph. H.. 1951> Sedimentary his tory of the Ventura basin, California, and the action of turbidity currents: Soc. Econ. Paleont. Mineralogy Sp. Pub. Wo. 2, p. 76-107- Otto, G. H., 19339 Comparative tests of several methods of sampling heavy mineral concentrates: Jour. Sedimentary Petrology, v. 3, p. 30-39- , 1933} Device for sampling heavy minerals: Geol. Soc. America Bull., v. Mf, p. 159 (Abstract). Pettijohn, F. J., 1939, Mineral analysis of sediments: Recent Marine Sediments, Am. Assoc. Petroleum Geologists Symposium, Editor P. D. Trask, p. 592-615. Reed, R. D., .92^, Methods for heavy mineral investigation: Econ. Geo., v. XIX, No. p. 320-337- , 19299 Sespe formation: Am. Assoc. Petroleum Geologists Bull., v. 13, p. ^89-507. Reed, R. D. and Bailey, J. P., 1927» Subsurface correla tion by means of heavy minerals: Am. Assoc. Petroleum Geologists Bull., v. 11, p. 359-368. : ................................................... 98 Reinhart, P. W.. 1928, Origin of the Sespe formation of South Mountain, Californias Am. Assoc. Petroleum Geologists Bull., v. 12, No. 8, p. 7U-3-7if6. Revelle, R. and Shepard, F. P., 1939, Sediments off the California coast: Recent Marine Sediments, Am. Assoc. Petroleum Geologists Symposium, Editor P. D. Trask, i p. 2if5-283. ’ ’ ! Rittenhouse, Gordon, 19*+3, Transportation and deposition of heavy minerals: Geol. Soc. America Bull., v. 5^, p. 1725-1780. ■ ______, 19^8. Analytical methods as applied in petrographic investigations of Appalachian Basin: U. S. Geol. Survey Circular 22, p. 1-20. ______, 1950, Detrital mineralogy. Symposium on subsurface geologic methods: compiled by L. W. LeRoy, Colorado School of Mines, p. I3I-I35. Rubey. W. W., 1933, The Size distribution of heavy minerals within a water-laid sandstone: Jour. Sedimentary Petrology, v. 3, p. 3-29. Smith, W. S. T., 1897, The geology of Santa Catalina Island: California Acad. Sci. Pro., 3rd ser., v. 1, No. 1. :Soper, E. K., 1938. Geology of the central Santa Monica Mountains, Los Angeles County, California: California Jour, of Mines & Geol., v. 3^-, p. 131-180. Sorby, H. C., 1851, On the microscopical structure of the calcareous grits of the Yorkshire Coast: Quart. Jour, of Geol. Soc., v. 11, p. 1. Storey. H. C., 19^7? Geology of the San Gabriel Mountains, California, and its relation to water distribution: State of California, California Forest and Range Experi ment Station, U. S. Forest Service, 19 p. Uchupi. Elazar, 195^> Submarine geology of the Santa Rosa Cories Ridge: unpublished Master’s thesis in geology, University of Southern California, 72 p. Woodford, A. 0., 1925, The San Onofre Breccia: University of California Bull. Geol. Sci., v. 15, No. 7, p. 159-280. APPENDIXES APPENDIX A MINERAL IDENTIFICATION IN SAND APPENDIX A MINERAL IDENTIFICATION IN SAND After a preliminary examination in immersion oils of ten widely spaced beach samples, it was possible to iden tify aroclor-mounted grains, using all, or some of, the following criteria5 habit, and remnants of crystal struc ture if any; transparency or opacity; relief relative to aroclor which has an index of refraction (N) of 1.66*f to 1.667; color and pleochroism; extinction angle and degree; sign of elongation; 2V angle and sign. The relief was estimated as follows: Negative relief = N lower than aroclor, for example, chlorite No relief * N equal to aroclor, for example, apatite Low positive relief = N between aroclor and 1.7, for example, augite Medium positive relief = N between 1.7 and 2.0, for example epidote High positive relief = N higher than 2.0, for example, rutile The following data were selected and compiled from standard textbooks in mineralogy: Epidote Formula - Ca2(Al-Fe, Al-Mn)^ (OH^i^O^ Form - Monoclinic. Habit - elongated and striated along the b* axis. Relief - medium positive. 101 102 Color - light green to lemon yellow, shades of brown, chips look like bottle glass with a remarkable transparency. Pleochroism - colorless to pale green. Extinction - parallel in longitudinal sections, inclined in transverse sections. Elongation - positive. Birefringence - strong, may be varying even in a single crystal thus giving a similar appearance to that of an aggregate polarization. Interference colors - in thick grains high, therefore appear much the same under crossed nicols as in ordinary light. Interference figure - BX (-) , 2V = 690 to 80 . Specific gravity - 3.25 to 3-37. Epidote is typically a mineral of low grade metamor- phic rocks, although it is present as a primary mineral in certain granites. It is common in gneisses, garnet rock, amphibolite, glaucophane schists, and phyllites, and as a contact mineral in limestone. It is also common as a secondary mineral, derived from feldspars, pyroxene, amphibole, biotite, and garnet, and Is frequently asso ciated with chlorite. Usually the two minerals, chlorite and epidote, form simultaneously from a common parent (Clark, 1959» P« *+11). Alterations due to weathering are rare (Winchell and Winchell, 1951s P* **50). Opaque Minerals Magnetite and ilmenite can definitely be separated from each other only if the crystal structure is clear or when the mineral is partly altered. Magnetite tends to turn into red hematite, whereas ilmenite tends to turn into white leucoxene. For the purpose of this study it seemed 103 better to lump all four minerals and use them as one species: opaque minerals (Table 7). Magnetite is very widespread in igneous and meta- morphic rocks. It is found sparingly in acid rocks but more abundantly in some basic types (Winchell and Winchell, 1951, p. 87). It is obviously most abundant in rocks which are rich in ferromagnesian minerals, such as norites, dia bases, gabbroes, or peridotites. Primary hematite is a product of contact metamorphism and occurs in various crys talline schists. It is common in many veins and as product of fumaroles near volcanoes (Winchell and Winchell, 1951, p. 62). Ilmenite is a common but sparse constituent of igneous rocks; not rare in metamorphic rocks and found in veins and alluvial sands (Winchell and Winchell, 1951, p. 6*f). It occurs in granite and syenite and as an essen tial constituent in diorite, diabase, gabbro, and basalt, and is also found in metamorphic rocks such as gneiss, mica schist, and amphibolite (Clark, 1959, p. 351). Pyroxene and Amphibole Pyroxene and amphibole (Table 8) can be divided into at least four species each, on the basis of their optical properties. For the purpose of this study, how ever, it seemed better not to subdivide beyond the species level; these minerals were treated as: pyroxene and amphibole species. TABLE 7.— Identification of onaaue minerals MAGNETITE HEMATITE ILMENITE LEUCOXENE FORMULA Fe3Oh FegO^ FeTiO^ .••Ti02 CRYSTAL Isometric Hexagonal Hexagonal Aggregate COLOR Blue-black Red Iron-black White, cream LUSTER High metallic None High metallic Dull ALTER TO Hematite Magnetite Leucoxene Rutile DENSITY ^.5 - 5.3 5.2 K5 - 5.0 — MAGNETISM Strong Very weak Moderate None +lOT TABLE 8.— Identification of pyroxenes and amnhiboles MIN E R A IJ PYROXENE X-SiO^ AMPHIBOLE X-Sig022 Augite Diopside Enstatite Hypersthene Hornblende Basaltine Glaucophane Act indite METAL Ca, Mg, Ca, Mg Mg Fe, Mg Ca, Mg, Ca, Fe, Na, A1 Ca, Mg Fet A1 FeT A1 A1 Fe CRYSTAL Mono Mono Ortho ......... Ortho Mono Mono Mono Ortho • HABIT Short prismatic Long prismatic STRIATION - - + + - - - - POT OR Bottle Green & None Pink & Dark Brown- Blue None wUJjUXI green gray green green black RELIEF Med. + Low + mm Low or Med. + Med. + - - med. + & - or & - PLEOCHROISM Green None None Red-yeL Green Yellow Blue- Yellow gray _ . -green green -brown green -green EXTINCTION >30° >30° 0 0 <30° <30° <30° <30° BX + + + m m M B - - - ALTER TO Amphibole etc. Chlorite etc. DENSITY 3.15 - 3.6 2.9 - 3.5 H O = = = = = 106 Pyroxenes are essential constituents of many igneous rocks and occur in nearly all such rocks. They are also found in various metamorphic rocks, both regional and con tact. They alter rather readily, especially to amphibole or chlorite (Winchell and Winchell, 1951, p. *+0*0. Amphi- boles are present in nearly all classes of igneous rocks and in many metamorphic rocks. They alter readily to chlorite, biotite, epidote, calcite, and talc (Winchell and Winchell, 1951, P. ^2*0. Biotite Formula - AlpMg2KHSi30i2 plus ferric and ferrous salts in variable proportions. Form - Monoclinic, almost hexagonal. Relief - usually is negative, but if high in Fe or Ti it may be medium positive. Color - brown or green. Pleochroism - colorless to brownish yellow. Extinction - parallel (only on edge). Elongation - positive (only on edge). Interference figure - BX (-), 2V near zero. Specific gravity - 2.7 to 3.4- . The specific gravity of biotite ranges from a little below acetylene tetrabromide to a little above it, hence its frequency in the heavies should be interpreted with reservation. Biotite is an important constituent of many massive igneous rocks such as granite, syenite, diorite, trachyte, andesite, and mica-basalt (Clark, 1959, p. 399), and of some metamorphic rocks such as gneiss and schist. It is a product of both regional and contact metamorphism (Winchell and Winchell, 1951, P» 376), and it alters readily to chlorite. 107 Chlorite Formula - (Mg, Fe, Al)6(OH)8(Si, Al)lfOio- Form - Monoclinic. Habit - micaceous, pseudo-hexagonal plates, perfect basal cleavage. Relief - negative. Color - dirty yellow green to green. Pleochroism - in thin grains, greenish shadows. Birefringence - low, compound (aggregate), or ultra blue. Interference figure - BX (+) or (-), seldom seen clearly, '2 V = 0°-30°. Specific gravity - 2.6 to 3.0. The frequency of this species, like that of biotite, should be interpreted with reservation due to the fact that the specific gravity ranges from "light" to "heavy.” Chlorite is not a single species but is a complex group of closely related minerals, the members of which are distinguished only with difficulty (Krumbein, et al.. 1936, p. **25). It is widely distributed in nature, being found in nearly all kinds of rocks, usually as an alteration product of biotite, pyroxene, amphibole, garnet, or olivine (Winchell and Winchell, 1951, p. 389). Chlorite is most abundant among the metamorphic schists. It can not form as a pyrogenic mineral and is always of secondary origin. When it appears in volcanic rocks it is as the result of hydrothermal alteration (Clark, 1959). Garnet (Almandi te) Formula - Fe Form - Isome Relief - medium positive 108 Color - pale pink. Interference figure - none (isotropic). Specific gravity - 3.9 to **.2. Almandite is the most widespread and persistent variety of garnet in detrital sediments (Milner, 191 +0, P* 233)- It is common in granitic rocks, gneisses and schists. Eclogite is a rock in which garnet and a green pyroxene are the principal minerals (Clark, 1959, p. *+06). Almandite alters readily to chlorite and epidote (Winchell and Winchell, 1951, p. ^89). Zircon Formula - Zr02Si02. Form - Tetragonal (ditetragonal dipyramidal). Habit - long prismatic along the c axis, often euhedral. Relief - medium positive. Color - yellowish to light brown, or no color. Pleochroism - none, may be in thick grains. Extinction - parallel. Elongation - positive. Interference figure - UX (+), or anomalous BX (+). Specific gravity - b*6 to k.7. Zircon is very widely distributed as an accessory constituent of all kinds of rocks, but it is especially common in syenite, granite, and diorite. It seems to be more abundant in plutonic than in volcanic rocks. It is also found in many kinds of metamorphic rocks (Winchell and Winchell, 1951, p. **95). Zircon is a very persistent mineral and has the index number one in Pettijohn^ "Order of persistence" (19^9, p. * + 89). Winchell (1951, p. ^95), describes it as remarkably resistant to alteration and attrition and there fore, he says, it can be traced through more than one cycle of erosion and sedimentation, and is a common accessory mineral of many sediments. Slatkin and Pomerancblum (1958, p. 5)> suggest that zircon is not as persistent as it is usually believed to be, when exposed to subaerial conditions or to fresh water circulation. Carroll (1953)9 pointed out that although zircon has no natural cleavages it is a brittle mineral, and can, in fact, be reduced in size by ordinary processes of weathering. Apatite Formula - CaijJ’CPOi*)^. Form - Hexagonal. Relief - none. Color - none. Pleochroism - none. Extinction - parallel. Elongation - negative. Birefringence - very low. Interference figure - UX (-). Specific gravity - 3.18. Apatite is widely, but sparsely, distributed in all kinds of rocks. It occurs most abundantly in regions of crystalline schists. It is usually quite fresh even when the enclosing minerals have undergone complete alteration (Winchell and Winchell, 19515 P. 199). Topaz Formula - (Al, F)pSiOi| . . Form - Orthorhombic. 110 Relief - negative, yellow red and blue (very close to aroclor). Color - none. Pleochroism - none. Interference figure - BX (+). Interference colors - striking yellow and red. Specific gravity - 3.5 to 3.57. Topaz is found especially in some rhyolitic rocks and greisen (R. H. Merriam, oral communication), and in contact zones and pegmatites (Winchell and Winchell, 1951 > p. 511). It may alter to kaolinite or sericite. Sphene Sphene, rutile, brookite, and anatase, are lumped together here under the species name: sphene (Table 9). The titanites are Widely, but sparsely, distributed in rocks of all kinds. Sphene is particularly common in horn blende granites, syenites, and diorites as well as in schists and gneisses. Rutile is common in metamorphic rocks such as amphibolite, eclogite, schist, and gneiss. Brookite and anatase are found in veins in igneous rocks and metamorphic rocks (Winchell and Winchell, 1951). Staurolites The staurolites (Table 10) are found chiefly in schists and gneisses, near contact of igneous rocks, and in pegmatites. This group includes staurolite, sillimanite, kyanite, and andalusite. All except sillimanite alter readily to mica, chlorites or sericite. ill! TABLE 9.— Identification of sphene and other titanium oxides MINERAL SPHENE RUTILE BROOKITE ANATASE FORMULA CaSiO^TiOg Ti02 Ti02 Ti02 CRYSTAL Monoclinic Tetragonal Orthorhomb Tetragonal COLOR Brownish yellow Red sub- metallic Straw yellow Pale pink Sub-metallic RELIEF Medium + High + High + High + EXTINCTION Incomplete Straight Incomplete FIGURE BX+ UX+ BX+, double UX- SPECIAL Ultrablue birefringe Extreme birefringe Strong striations & cross " Strong stria tions, weak cross stria. ALTER TO Leucoxene Ilmenite DENSITY 3.^3.56 b.2 3.87-if.l 3.82-3.97 112 TABLE 10.— Identification of staurolites MINERAL STAUROLITE SILLIMANITE KYANITE ANDALUSITE FORMULA Al203Si02 + HFe Al203Si02 Al203Si02 Al203Si02 CRYSTAL Orthorhomb Orthorhomb Triclinic Orthorhomb COLOR Straw yellow None None Pale shades RELIEF Medium + Low + Low + -, yellow and blue PLEOCHROIC Yellow- colorless Brown-green -blue Blue- colorless Rose pink- colorless EXTINCTION Straight Straight Inclined Straight ELONGATION + + - FIGURE, BX 2V+ large 2V+ small 2V- large 2V- large DENSITY 3.65-3.77 3.25 3.6 3.1-3.2 113 Olivine Formula - MgFeSipO^. Form - Orthorhombic. Fructure - conchoidal. Relief - medium positive and, in the same grain, nega tive. Color - green. Pleochroism - none. Birefringence - vivid colors. Interference figure - BX (+). Specific gravity - 3.2 to Olivine occurs in basic and ultrabasic igneous rocks commonly associated with augite, plagioclase, hypersthene, magnetite, etc. It is altered very readily and may be partly or fully transformed to serpentine or iddingsite (Winchell and Winchell, 1951, p. 501). APPENDIX B STATION LOCATIONS APPENDIX B STATION LOCATIONS Sample Number Location Age and Formation Analyzed by Al Point Mugu Beach Recent Aut B1 Sycamore ii it it Cl Little " ii ii ti D1 Trancas it ti it El Westward ii it ii FI Escondido n n ii G1 Coral it it ii HI Malibu ii it ii 11 Big Rock it it ti A3 Topanga it n it B3 Will Rogers ii it it C3 Redondo ii it ti 07 Little Sycamore Canyon ii ii E 7 Venice Beach n tt F 7 El Segundo ti •i n G 7 Marineland it it it H7 Pt. Fermin it it ti H9 Imperial Hwy,, and L. A. River n ii Cll Downey St, and L. A. River it it Dll Main St, and L. A. River tt n Gil San Qnofre Beach it ii Hll San Clemente it n ti 111 Capistrano n tt tt A13 Aliso ti ti tt B13 El Morro n ii tt C13 Corona Del Mar 1 1 tt it D13 Newport it ti ti E13 Huntington ti it it F13 Bolsa Bay ii it ii G13 Seal H ti it H13 Bluff Park it ii tt 113 AHF 50^3 34-03-20 N 118-58-4-5 W Offshore it it 115 STATION LOCATIONS (Continued) Hi Sample Number Location Age and Formation Analyzed by Al? AHF ?693 3*+-o2-io N Recent Author Bl? 118-?8-h-? W Offshore AHF ?OlfO 3*+-00-20 N ti ti 119-01-00 W ti t i ti Cl? Scripps Beach it n Dl? Pacific ti ti tt El? Ocean tt ti ii PI? Coronado ti n t i Gl? Silver State ii it i t m? Imperial tt it i t 11? Point Loma it ii ii A17 Torrey Pines it i t it B17 Solana it ti i t C17 Moonlight it i t i i D17 La Costa ii ii it E17 Carlsbad t i it ii F17 Oceanside i t i t ti G17 H17 Las Floras AHF ?709 33-?6-0? N ii t i ii 117 118-27-22 W AHF ?097 N Offshore it n A19 118-28-02 W AHF ??38 33-?h-26 N it i t ii B19 118-29-37 W AHF ?099 33-?3-?8 N n t i i t C19 118-31-26 W AHF 5100 33-?3-3? N it it i t E19 118-33-10 W AHF ^-719 33-^1-?8 N ti tt i t FI 9 118-07-^3 W AHF ?7?2 33-lfO-30 N n ti n G19 118-09-30 W AHF *t882 33-38-36 N n ii i t 118-00-07 W ti ii ii 117 STATION LOCATIONS (Continued) Sample Number Location Age and Formation Analyzed by 119 AHF 5744 33-36-48 N 118-08-35 W B21 AHF 5748 33-34-45 N 118-11-4-0 W C21 AHF 574-7 33-33-48 N 118-11-45 W D21 AHF 4930 32-38-00 N 117-09-00 w E21 AHF 4929 32-38-00 N 117-11-00 W F21 AHF 4932 32-38-00 N 117-13-00 W G21 AHF; 4934 32-38-00 N 117-15-00 W H21 AHF 4913 32-36-00 N 117-18-30 W 121 AHF 5314 34-26-40 N 120-24-15 W A23 AHF 4941 34-26-10 N 120-24-20 W B23 AHF 5558 34-25-10 N 120-24-00 W C23 AHF 4940 34-25-20 N 120-24-12 W D23 AHF 4939 34-23-20 N 120-24-30 W E23 AHF 5559 34-23-08 N 120-23-15 W F23 AHF 6249 N — — W Offshore Recent Author n n it it tt tt t i it tt tt tt tt ti tt it it tt tt tt tt t t tt 118 STATION LOCATIONS (Continued) Sample Number Location Age and Formation Analyzed by C25 Gaviota Beach Recent Author D25 San Augustin n t« tt E25 Tajiguas 1 1 1 1 t i F25 Capitan it 1 1 1 1 G25 Goleta «i 1 1 1 1 H25 Hendrys it 1 1 1 1 125 Santa Barbara it ti ti A27 Loon Point n it ti B27 Carpinteria 1 1 1 1 ti C2 7 Punta Gorda it 1 1 tt D27 Pitas Pt. 1 1 it it E27 Taylor Ranch it it tt F2 7 Ventura Dump 1 1 1 1 1 1 G27 Fifth St. 1 1 1 1 1 1 127 A33 Port Hueneme AHF 5+936 32-5+0-00 N tt 1 1 n B33 117- 19-00 W i AHF 5613 32-5+0-5+5 N Offshore 1 1 1 1 C33 117-18-30 w AHF h79*- 32-5+2-00 N 1 1 n ti D33 117-17-55 w AHF 5076 32-5+2-5+5 N it it 1 1 E33 117-16-4-5 W AHF 4-758 32-51-50 N 1 1 it it F33 117-15-5+0 W AHF 4-757 32-52-00 N it it 1 1 033 117-18-00 W AHF 4-756 32-51-55 N ti it n H33 117-20-30 W AHF 4-861 33-05-4-5 N 1 1 n 1 1 133 117-19-20 W AHF 5+859 33-05-5+0 N ti 1 1 it A35 117-21-00 W AHF 5+858 33-05-5+5 N it 1 1 ■ n 117-23-30 W it ti 1 1 119 STATION LOCATIONS (Continued) Sample Age and Analyzed Number___________hoc&zion___________ Formation by B35 AHF 5633 32-22-50 N 117-1*1-20 W Offshore Recent Author C35 AHF 5632 33-22-50 N II7-39-OO W " " D35 ahf 4772 33-21-35 N 117-38-05 w * » " It E35 ahf 5630 33-22-05 N 117-3^-55 w " . « « F35 ahf 5211 33-30-50 N 117-1 *9-05 W « ” " 035 ahf 1 * 871* 33-31-35 N 117-1*7-58 w « » « * ' H35 AHF *+779 33-32-00 N 117-1*7-1*0 w * ' « « 135 AHF 5657 33-32-18 N 117-1*7-15 w " » » » A3 7 AHF 5701 33-58-50 N H8-if6-10 W " " " B37 AHF 5702 33-59-18 N 118-1*6-10 W M tt « » C37 AHF 5703 33-59-50 N 118-1*6-10 W " " » « D37 AHF 570^ 3^00-15 N 118-1*6-10 W • » » « E37 AHF 5705 3i*-00-55 N 118-1*6-25 W • * ' • " F37 AHF 5683 3l*-0lj-30 N 119-12-50 W « " « G37 AHF 5682 3l*-05-l*2 n 119-13-03 W " « " 1201 STATION LOCATIONS (Continued) Sample Number Location Age and Formation Analyzed by H37 AHF 5681 31+-06-U-7 N 119-12-58 W 137 AHF 5528 3^-07-25 N 119-12-20 W A39 AHF 5529 31 f-07-50 N 119-12-33 W B39 AHF 5530 31+-08-30 N 119-12-^-5 w C39 AHF 533^ 3^-18-4-0 N 119-21-10 W D39 AHF 5335 3^-15-58 N 119-21-M-5 W E39 AHF 5336 3^-15-15 N 119-22-22 W F39 AHF 5338 N 119-23-50 w G39 AHF 5339 3^-13-02 N 119-2M--35 W H39 AHF 53^-0 3^-12-15 N 119-25-30 W 139 AHF 54-17 34—22-00 N 119-31-25 W Al+1 AHF 5**16 3^-20-55 N 119-31-20 W BH-1 AHF 5^15 3‘ f-19-l f5 N 119-31-15 W C*fl AHF 5586 3^*18-55 N 119-32-10 W Jhl AHF 571b 3^-17-00 N 119-32-25 W Offshore Recent Author 1 1 1 1 it 1 1 1 1 it n it n 1 1 121 STATION LOCATIONS (Continued) Sample Number Location Age and Formation Analyzed by E*+l F*+l G*+l H*+l I*+l A^-3 bM- 3 c * + 3 D*+3 e ? + 3 F*+3 G*+3 H*+3 A*+5 B*+5 Offshore ti tt tt AHF 5590 3*+-ll+-i+5 N 119-32-10 w AHF 5570 31 +-23-20 N 119-^2-00 W AHF 5309 31^23-05 N 119-1+3-00 W AHF 5571 3*l-21-*+2 N 119-^3-00 W AHF 5310 3*4-21-20 N 119-^3-00 W AHF 5311 3I+-I9-35 N 119-^-3-20 W AHF 556k 3^-27-1+5 H 120-12-32 W AHF 1+938 3*4-27-25 N 120-12-55 W AHF 5563 31H.26-30 N 120-12-32 W AHF 5312 3*+-26-20 N 120-12-35 W AHF 63*$ 32-37-3O N 119-27-50 W " Basin AHF 6351 32-01-00 N " » 119-23-00 W Anacapa Island Beach AHF 598*+ 3*1-12-50 N 120-00-05 W Offshore ' • AHF 21+90 33-3I +-28 N 119-50-58 W " Bank Recent Author tt 122 STATION LOCATIONS (Continued) Sample Number Location Age and Formation Analyzed by D k-5 F^-5 Gl+5 H^-5 Ab7 Bh7 c k-7 D b7 Baldwin Hills on La Cienega Avenue south of Rodeo Street Baldwin Hills at Cloverdale Street and Terrace Drive AHF 5225 3^-01-05 N 119-32-30 W Santa Cruz Island Smugglers Cove Beach AHF 5232 33-52-^f8 N 120-02-10 W Santa Rosa Island South Point « AHF 523*+ San Clemente Island Wilson Cove " San Clemente T8S, R6W, SBBM San Clemente T8S, R6W, SBBM San Clemente T8S, R7W, SBBM San Clemente T8S, R7W, SBBM San Clemente T8S, R7W, SBBM San Clemente T8S, R7W, SBBM Upper Pliocene sandstone, at Pleist. con tact Pleistocene beach sand with bedding and cross bedding Recent Upper Creta ceous Upper Schulz Mem. Williams For mation Paleocene Middle Section Silverado Fm. Up. Middle Eocene Santiago Fm. Lower Miocene (or Up. Olig.) Vaqueros Middle Miocene Sand lense in San Onofre Breccia Upper Miocene Mid. Monterey Fm. Author 1 1 t i ti 1 1 1 1 n 1 1 ti 123 STATION LOCATIONS (Continued) Sample Location Age and Analyzed Number Formation by E^-7 San Clemente Quaternary Fb 7 T7W, R7S, SBBM AHF 2730 33-IfO-OO N Stream terrace Author Qh? 118-36-00 W Offshore Basin AHF 512M- 33-16-20 N Recent n Hh-7 119-58-00 W " AHF 4-710 33-50-55 N 1 1 n Ik-7 119-04-35 w " AHF 4-690 33-30-14- N 1 1 it Ab9 118-22-25 W 1 1 1 1 1 1 Elysian Park Middle Miocene B*f9 Santa Monica Mountains Sand it Elysian Park Santa Monica Mountains Middle Miocene Sand, Topanga Fm. 1 1 Cl+9 Elysian Park Upper Miocene Dif9 Santa Monica Mountains Modelo Fm. tt Malaga Cove Upper Miocene Eb9 Palos Verdes Malaga Mudstone 1 1 Chandlers Quarry Lower Pleistocene Fb9 Palos Verdes AHF 5128 33-^5-30 H San Pedro Sand ti Cft-9 119-12-30 W Offshore Bank AHF 5138 33-36-40 N Recent 1 1 H»f9 119-02-32 W " " AHF 2902 Santa Barbara n 1 1 1^9 Island Beach AHF 2098 Catalina Island it 1 1 A5l Emerald Cove Beach AHF 184-7 Catalina Island 1 1 n B£L White Cove Beach AHF 1984- 32-37-04- N 1 1 1 1 118-07-35 W Offshore Basin tt ti i STATION LOCATIONS (Continued) Sample T .n n a +;H n n Age and Analyzed Number Formation by C51 AHF 1982 32-16-00 N 119-18-45 W Offshore Basin Recent Author D51 AHF 1883 32-30-19 N 119-13-25W 1 1 Bank n n E51 AHF 2182 32-59-36 N 118-58-20 W 1 1 Basin n 1 1 F51 AHF 1941 33-44-10 N 119-30-30 W 1 1 ti it it G51 AHF 4695 32-12-38 N 119-26-43 W n it it H51 AHF 4671 32-19-00 N 118-38-00 W n n n 1 1 151 AHF 4672 32-07-30 N 117-56-00 W AHF 4667 ti 1 1 n it A 53 32-35-42 N 117-32-43 W ” Trough 1 1 n B53 AHF 1983 32-12-30 N 118-19-30 W n Basin 1 1 11 C53 AHF 199o 32-3^-30 N 120-00-40 W 1 1 1 1 11 D53 AHF 4673 31-5^-00 N 118-11-00 W 1 1 tt 1 1 1 1 B53 Malaga Cove Lower Pliocene Palos Verdes Repetto Shale 1 1 F53 AHF 4820 34-24-50 N 120-28-10 W Offshore Recent 1 1 G53 Point Loma San Diego Cliff Cretaceous, Lower Upper Chico Sandstone it H53 Point Loma ti Cretaceous, Mid Up. Chico Sand • San Diego Matrix in Cgl. " i -.......J 125 STATION LOCATIONS (Continued) Sample Number Location Age and Analyzed Formation by 153 Point Loma Cliff San Diego A55 Point Loma Cliff San Diego B55 Topanga Canyon Santa Monica Mts. C55 Topanga Canyon Santa Monica Mts. D55 Topanga Canyon Santa Monica Mts. E55 Topanga Canyon Santa Monica Mts. A57 Elysian Park Santa Monica Mts. B57 Elysian Park Santa Monica Mts. C57 Elysian Park Santa Monica Mts. D57 Elysian Park Santa Monica Mts. E57 Elysian Park Santa Monica Mts. F57 Elysian Park Santa Monica Mts. HA1 Carpinteria Beach (B27) HA7 Punta Gorda " (C27) HA8 Rincon » HA9 Rincon Park * * HA10 Solimar " HA11 Taylor Ranch 1 1 (E27) HA13 Ventura River HA15 Ventura Park HAlo Ventura Dump (F27) HA20 Fifth St. Beach (G27) Cretaceous, Upper Upper Chico Sandstone Pleistocene, an unconsol idated Sd. on lower Terrace Lower Miocene Vaqueros Fm. Middle Miocene Topanga Fm. Paleocene, Martinez Fm. Oligocene, Sespe Fm. Middle Miocene Sand Middle Miocene Sand Middle Miocene Sand Upper Miocene Sand Upper Miocene Sand Upper Miocene Sand Recent Author Handin (1951) 1 1 t i ti t i it it 1 1 it it t t it 1 1 tt t i it STATION LOCATIONS (Continued) 126 Sample Number Location Age and Formation Analyzed by HA23 Port Hueneme , Beach Recent Handin HA26 (127) Mugu Swamps tt tt Ug5D HA27 Colleguas Creek tt tt HA28 Point Mugu (Al) Seqult Pt. tt tt tt HA36 it 1 1 It HA37 Sycamore (Bl) it 1 1 It HA39 Lacus Pt. n tt It HA40 Trancas (Bl) tt tt It HAM* Westward (El) n it tt HA53 Coral (Gl) tt tt tt HA 56 Malibu (HI) 1 1 it tt HA59 Big Rock (11) tt tt tt HA63 Castle Rock tt tt It HA66 Will Rogers (B3) tt tt 1 1 HA72 HA7^ Venice (B7) Ballona Creek and Sepulveda Blvd. tt tt tt tt It HA75 Dockweiler tt tt tt HA78 Redondo (C3) Malaga Cove tt tt tt HA82 tt 1 1 It HA8^ Pt. Fermln (H7) tt tt tt T712 T713 Jalama S. Point tt tt Trask (1952) T71b Conception N. Point it it tt T715 Conception tt tt tt Whale tt it 1 1 T723 T72*f Hendreys tt tt tt Eldwood tt it tt T7**7 Gaviota tt 1 1 it T801 East tt tt tt 127 STATION LOCATIONS (Continued) Sample Location Age and Analyzed Number Formation by T8ll West Beach Recent Trask T936 (1952) Jalama River it it T966 San Jose Creek tt it I993 T99H* Santa Ynez ' it tt River tt it it n T99- Gavlota Creek tt it T996 Dos Pueblos n 1 1 n 1997 ti n 1 1 n it T1001 San Hoque ti tt 1 1 T1005 Santa Ynez River it it T1006 Jalama n 1 1 it T1007 Santa Ynez Beach 1 1 it LAI Santa Margarita Mts. Jurassic, Grano- Larsen diorite porphyry (19^8) (p. 29) LA 2 II H 1 1 it ti 1 1 LA3 II tt tt 1 1 n it LA4- San Marcos Mts. Cretaceous Olivine gabbro Larsen (19W LA5 San Marcos 1 1 Cretaceous (p. w Norite (gabbro) tt LA6 San Marcos it Cretaceous Qtz-biotite nor ite (gabbro) tt LA7 San Marcos it Cretaceous Hornblende (gabbro) ’ • LA8 Woodson tt Cretaceous Granodiorite Larsen (19^8) (p. 78) LA9 Poway Grade Cretaceous Larsen Granodiorite (19^8) (p. 81) LAIO Lancaster Mt. Cretaceous Larsen (Indian Mts•) Leucogranodiorite (19H-8) (p. 86) LA11 Escondido Creek Cretaceous Larsen Dlegulto Creek Leucogranodiorite (19W (p. 89) LA12 Mt. Hole Jurassic, dike, Granodiorite porphyry Larsen (19^8) (p. 91) LA13 Tertiary volcanic Mesa basalt Larsen (19*+ 8) (p. 110) STATION LOCATIONS (Continued) 128 Sample Location Age and Analyzed Number Formation by LAI1 * Santa Ana Mts. (Average of LA8 and LA9) Larsen (19 W LAI 5 i t t t i t Triassic Slate t t LA16 tm (Average of LAI, 2, 3, 8, 9) , t t LA17 (Average of LA1 *, 5, 6, 7) 1 1 BM3 San Diego Co. Tertiary (?) Bellemin Fairmont Rd., N. of Soda rhyolite and El Cajon Blvd. tuff Merriam Poway conglomer ate (1958) BM1 * San Diego Co. U. S. Hwy. 395 Tertiary (?) Rhyolite tuff Poway conglomer ate i t BM5 San Diego Co. Sorrento Miramar & Linda Vista Rds. Tertiary (?), Soda rhyolite porphyry, Poway BM6 conglomerate i t San Diego Co. U . S. 395 N. of Carrol Canyon Tertiary (?), Soda rhyolite porphyry, Poway conglomerate i t BM7 San Diego Co. Ridge N, W. of Lake Tertiary (?) Soda rhyolite BM8 Murrey Blvd. tuff, Poway conglomerate t t San Diego Co. Lakes ide-Ramona N. of Barona turn Tertiary (?), Soda rhyolite tuff, Poway conglomerate i t Gil Ventura Co., State Hwy. Oligocene Gianella 150 E. of Ojai Sespe Fm. (1928) DAI Santa Barbara Co. Jurassic Along Santa Ynez River Franciscan schist Davis (1918) DA2 i t t t t t i t t t DA3 t t t t t t t t t t ST1 San Gabriel Mts. Jurassic, Granodlarite Strong (1905) ST2 i t t i i t Jurassic (?), Dike Qtz.-hb.- porphyrite t l _______________. . ___. . . . ________________________ ... 12 9; STATION LOCATIONS (Continued) Sample Location Age and Analyzed Number Formation by ST3 San Gabriel Mts. Jurassic (?) Strong Hb.-diorite- (190?) ST*f gneiss t« ii it (Average of 2 and 3) it HGl? San Diego Lower Pliocene Hertlein San Diego Em. and Grant (19^) HG16 it n ii II HG18 i i ti ti II HG19 tt it Upper Pliocene Sweitzer Fm. II EMI Coronado Strand Recent Emery et al. (1952) EM2 Los Coronados Isl. it It EM3 EMfr Coronado Bank ii II La Jolla Cretaceous II EM5 « it Eocene sand II EM6 n it Eocene, Torrey sand 1 1 EM7 it ti Eocene, Rose. EM8 Cnyh sand II Pacific Beach Pliocene, San Diego Fm. II EM9 N. Coronado Isl. Miocene II EM10 Point Loma Cretaceous shale It EM11 Los Coronados Isl. Eocene sandstone II EMI 2 Coronado Bank Pliocene • ' 1 1 EM13 Coronado Bank Pliocene shale It EMlH- Los Coronados Isl. (Average of EM2, EMI 5 9, 11) II La Jolla Eocene (Average of EMJ>, 6, and 7) 1 1 APPENDIX HEAVY MINERAL FREQUENCIES C IN PER CENT APPENDIX C HEAVY MINERAL FREQUENCIES IN PER CENT All the mineral frequencies are rounded to the nearest percent. The percentage of heavies in the total sand is rounded to the nearest tenth of a percent. The following symbols are used all through this appendix: EP - Epidote OP - Opaque minerals AM - Amphibole PX - Pyroxene BI - Biotite CH - Chlorite GA - Garnet ZI - Zircon TO - Topaz AP - Apatite SP - Sphene ST - Staurolite Ot - Other minerals %E - Percentage of heavies - - Figure not available # - Olivine * - More than 50% pyrite Sample M i n e r a 1 s Number EP OP AM PX BI CH GA ZI TO AP SP ST ot % H A1 16 kk 10 k 2 2 0 1 2 2 0.8 Bl 11 *+0 5 6 11 k 2 1 2 1 k 0 13 3.0 Cl 2k 38 6 2 — m . k k 1 3 k 0 7.9 D1 k? 23 10 2 — — 2 k 1 1 2 0 w 3.8 El 25 3 1 6 10 k 0 2 1 k 0 10 0.8 FI 38 ko 1 6 6 3 2 1 0 2 1 0 0 1.3 G1 38 35 3 0 k 6 2 1 3 0 3 0 5 1.2 131 132 HEAVY MINERAL FREQUENCIES IN PERCENI (Continu 1 s ed) Sample Number M I n e r a EP OP AM PX BI CH GA ZI TO AP SP ST ot % H HI 28 30 10 1 12 6 1 1 3 3 1 0 4 4.2 11 35 34 6 1 5 4 4 0 1 5 4 0 0 3.7 A3 M i - 14 12 2 6 5 1 1 0 0 0 2 13 3.1 B3 27 34 8 2 6 7 3 1 3 0 4 0 5 3.1 C3 21 49 4 0 4 8 0 0 0 2 0 0 12 12.2 C 7 5* 14 8 2 2 0 0 0 0 1 0 1 18 8.5 E7 20 38 8 3 9 10 3 2 3 1 2 1 0 3.3 F 7 25 25 14 2 9 13 0 0 2 0 1 0 9 3.4 G 7 0 16 0 0 0 0 0 0 76? 8 0 0 0 7.3 H7 18 26 28 5 5 15 5 0 0 1 0 1 0 1 2.5 H9 8 64 11 5 4 1 1 0 0 1 0 0 2.6 Cll 28 37 17 8 2 4 0 0 2 1 1 0 0 2.7 Dll Gil 15 17 11 4 6 1 9 x7 1 0 0 0 1 0 0 2 1 0 1 0 11 6 0.4 0.1 Hll 20 25 20 7 3 14 2 0 0 0 0 8 1 0.8 111 15 37 13 6 2 9 0 1 0 0 2 0 15 3.7 A13 h-5 18 5 3 1 9 2 0 1 0 4 2 10 2.4 B13 20 20 24 9 1 5 4 0 1 0 1 1 14 0.1 C13 23 7 26 13 0 10 1 0 0 2 2 0 16 3.9 D13 24 10 10 5 6 3 1 1 1 1 2 17 0.9 E13 21 18 4 21 5 14 2 2 2 0 1 1 10 3.2 F13 19 12 14 24 6 14 1 0 0 0 0 0 10 1.2 G13 15 17 11 16 3 0 0 0 0 0 2 21 4.6 H13 19 22 35 9 6 4 0 1 0 2 2 0 0 9.9 113 29 14 14 7 - - 2 1 5 0 0 0 — 0.2 A15 31 9 6 - - 3 2 0 2 0 0 — 0.1 B15 47 17 38 2 — - 1 2 0 1 2 0 - 0.04 C15 10 10 6 0 2 0 1 3 4 3 0 23 7.0 D15 ? 1 35 9 23 9 0 0 3 0 0 3 8 1.1 E15 4 11 50 20 0 2 1 2 l 0 1 2 6 0.7 F15 2 18 33 11 23 3 0 4 l 0 0 1 4 7.0 G15 4 7 49 7 12 5 0 0 0 0 1 2 13 9.2 HI 5 5 7 50 12 8 13 0 0 0 0 0 1 0 6.3 115 9 29 40 7 0 0 6 0 0 0 1 1 7 2.4 A17 8 4 26 9 15 12 0 3 1 1 5 2 14 20.6 B17 9 9 31 8 7 10 1 0 1 1 l 0 22 7.0 C17 10 2 29 11 9 12 1 0 0 2 3 2 19 6.7 D17 8 4 34 14 8 19 0 0 0 2 0 0 11 2.7 E17 7 11 29 7 14 17 2 1 0 1 l 0 19 22.9 F17 9 10 22 7 14 25 0 0 1 1 1 1 9 0.9 G17 8 5 22 8 13 26 0 0 0 1 0 0 17 0.7 H17 17 55 2 1 3 4 3 0 0 1 0 0 14 0.3 117 33 24 11 4 0 2 1 0 1 2 3 0 19 1.1 HEAVY MINERAL FREQUENCIES IN PERCENT 133 (Continued) Sample Number M i n e r a 1 s EP OP AM PX BI CH GA ZI TO AP SP ST Ot % H A19 27 10 28 8 0 1 0 2 1 3 0 0 20 hi B19 10 45 5 3 0 12 1 0 0 l 1 0 22 6.5 C19 13 21 9 11 0 11 0 0 0 2 1 0 32 0.9 El 9 16 17 28 8 1 1 2 1 0 3 1 0 22 5.0 F19 18 5 20 11 2 6 1 1 2 2 1 0 29 4.6 G19 28 6 36 13 1 1 0 0 1 4 1 0 9 1.9 119 23 10 16 5 3 8 1 0 4 2 0 0 28 4.5 521 27 16 23 9 2 3 0 0 2 2 2 1 13 3.5 C21 12 13 23 8 6 3 0 0 0 4 2 1 28 2.5 D21 6 7 32 16 6 2 0 0 1 2 1 0 27 8.5 E21 3 5 42 21 5 2 1 0 3 2 2 0 26 5.8 F21 7 19 40 15 1 0 0 3 1 0 3 0 11 4.7 G21 4 9 30 13 11 3 0 0 0 4 0 0 26 2.3 H21 5 3 3.6 15 0 6 0 1 2 5 l 0 26 2.0 121 19 22 4 0 15 11 2 0 1 2 3 0 21 0.2 A23 24 45 0 0 3 11 3 10 0 1 2 1 0 0.6 B23 33 36 0 0 1 3 13 11 0 0 3 0 0 0.8 C23 39 3£ 1 0 2 0 16 10 0 0 2 0 3 1.3 D23 38 28 2 0 0 0 10 6 0 0 2 0 14 1.1 E23 37 37 0 0 1 o 5 3 0 1 2 0 14 0.3 F23 7 23 3 1 26 0 0 0 0 9 0 0 31 3.3 C25 23 26 1 0 1 12 2 1 3 7 5 10 9 0.1 D25 23 47 0 0 0 o 5 2 0 0 3 4 16 0.8 E25 32 45 0 0 1 8 5 2 2 0 3 2 0 0.2 F25 43 27 1 1 5 6 3 2 5 1 2 4 o 0.1 G25 hi 28 2 0 5 3 4 1 6 0 3 3 4 0.1 H25 26 51 1 2 4 11 1 1 0 2 1 0 0 0.1 125 21 28 1 0 10 3 7 1 10 4 9 6 0 0.1 A2 7 3S 3S 3 0 4 1 3 1 4 3 2 1 14 0.1 B27 38 28 1 1 1 6 2 0 0 5 3 2 13 0.1 C27 21 bO 0 0 6 3 4 2 8 5 4 4 3 0.3 D27 10 ?? 1 2 1 7 0 1 9 7 1 1 0 0.1 E27 39 bb 0 0 2 2 7 0 0 1 3 2 0 0.5 F27 20 21 14 5 1 13 2 0 0 1 7 3 13 0.1 G27 28 21 7 3 31 0 2 1 0 1 4 2 0 0.2 127 21 2b 6 11 7 9 1 1 2 0 2 1 15 1.0 A33 3 1 38 4 2 7 0 0 2 5 2 0 36 7.4 B33 3 7 38 4 13 7 0 0 1 3 0 0 24 6.7 C33 2 7 30 8 19 4 o 0 2 4 1 o 23 6.5 D33 8 27 22 6 0 2 0 2 2 0 0 0 31 17.1 E33 11 11 33 5 0 8 1 0 0 2 1 0 28 10.6 F33 9 8 29 3 6 4 2 0 1 3 1 0 34 3*5 G33 6 2 24 3 5 1 1 0 1 1 1 0 54 5.3 H33 10 4 31 2 10 1 0 0 1 1 0 0 4o 9.8 _____ _____ ...... . J- co |H ■p fl o o EH & eq o M CQ W M o* M a w PQ © H © f i » - 9 a g © 3 CO s UN OVTNC^lNUNO INv O UN C M COH C " « C M rOOvJj-J* J - COJ- cO C M O U nO O C O O U nIN C M C M OnO nC s.UnC n.UnIN.O INOn • • * • • • • • • • • • « • • • • • • • • • • • • « • • • • • • • • • • • • • • • • • COCMHcO<MUncOCMJ- N W W N H H r l r l H f O O H H H H H H H O O v O H H W O O O O O O O H O W O COCOH IN H C V IU N V O H H O O J - O OCOvQ O Q OvOOOUNH C M H vO H UncMCOv O C M 00 O N C O t>- c o c o c o j- c o c o c o j" C M C M CMcocO cOCM H H H H ^ f O W f O C M H c o H C M cocoCM C M cocoCM O O O O O O O O O O O O O O O O O O O C M O O O O O O O O O O O O OJ- H H O H O O H O O H H C M O O H W H H C M H H H H H C M C M H H W O I r O H O H H O H HUNCM HCO C M C O C M C M H H COH COO O OCM-±COCMMDOvOCMmCM COCOUXd-J- O N COH CMUNrOO-H O C M C M J* O H ® cO ud* J - C M O rO O H C M H H H H r l H r l C M H H iH UNrl C M O O C M O H C M C M H H C M O H O C M H H UNCOO H O O O O H H H O H O O O O O O O H O H O © O O O O O O O C M H O H H O O C M H OJ- O H H H O O O O O H H H O O H H C M C M C M J* C M H H O H O O O O H O H COCOO H H O O C M C M H J - CM CMHHOOOO fO H J - H O H r l cO H c o U \j - UncM Un O Un UnUnJ - Cv-UNONJ- J - H j - UNH H C M i>-COCM C M CO C JN vO COud-vO vO O UN C M UN H C M O CO CO CM H C M COH O H O H H On C M CSHvO C M C M COH O cOcOINONCO O-tN-U) C M J* U N C O C M C M M 5 C M ca± C D C0J- O J - C M vO J - H UnH H C M H H CM U nC M C M C O C M H J - J - H C M C O C M C M UNvO C M C M C M O C M H C M COH C M O U ncoC M H n O UNCO n O UnJ - H H H H J - H H C M C M H H O O O O O rOH H C M H H C O H vO J-C SvO U M S.rO U vJC M j-C O rO vO CMUNINO Jr rO O H HvO H O H CMUncOH O H H H COCOCM H C M H CO CM H C M UN HvO C M tNCO C O C O H C M OCO O I S O H J - COCOUNCO UNCM c o d ’ COOOUnO H O v OCO C O C M O O H C M H coU n v O H HCMCMCMCMCMHCMCMH C M J* CMCMHCMHHHHHHCMH C M C O C O H C O C M H H H IfNCM O C M H C M J * cOCOvO C M O OCMUMN.J- On C M CO COvO v £ > COH IN J- C n - O v O H U N H J- O H J-C O O J - U n h c * 0 H H H H H C M H COCOCM C M C M COH H COH COCO H C M H C O C M C M cOCOur C M C M COCOCOUn rOUNUNUNUNUNUNUNUNUNCNCN.CNlNCN.tN.l>.CN-CN.OOOONOOC3NOOH H H H H H H H H COCOCOCOCOCO CO CO CO CO CO c o c o CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO co c o CO co J - j * j - J - J d : J*-d" j* - d -j - j * - d - j - j - H p q o O p q O W h « d p q o Q H fo © W h « s { c q o « W P h © W h m o A H f r a W h oQpqpt, HEAVY MINERAL FREQUENCIES IN PERCENT (Continued) 135 Sample Number M i n e r a 1 s EP OP AM PX BI CH GA ZI TO AP SP ST ot % H (*-3 .25 37 8 1 2 0 0 0 0 3 0 0 24 0.07 H43 85 14 1 0 0 0 0 0 0 0 0 0 0 1.6 A45 20 59 4 1 3 1 0 0 1 3 0 0 8 1.7 B45 3b 14 2 2 0 1 5 2 1 2 2 0 35 0.2 C45 1 qU ■ — / * 2 0 0 1 0 2 0 0 0 0 0 0.1 D45 1+1 4l 11 0 0 0 2 0 0 0 0 0 5 0.6 E45 82 16 1 0 0 0 0 0 0 0 0 0 1 1.4 F45 25 52 2 2 0 1 6 0 0 0 3 0 9 0.3 g45 39 lb 6 7 0 0 6 0 0 1 4 0 23 0.02 H45 13 7 13 5 33 0 0 1 0 0 0 0 28 1.2 145 0 99 0 0 0 0 0 0 0 0 0 0 0 1.7 AU-7 83 12 1 0 0 0 1 0 0 1 1 0 2 0.2 b47 6b 13 9 2 0 0 0 0 0 0 0 0 12 0.01 CM-7 34 12 21 9 0 0 0 3 0 0 0 0 21 3.2 D47 15 19 19 5 0 0 5 1 4 3 0 0 29 0.1 E47 40 13 19 l 0 0 0 1 0 0 0 0 26 0.2 F47 5 78 0 1 2 12 0 0 0 2 0 0 0 25-5 G47 23 20 9 4 10 0 2 0 0 0 0 0 32 0.2 % 7 36 16 12 2 0 7 2 1 0 0 1 0 23 0.2 147 17 l1 * 9 20 0 0 0 0 0 1 1 0 38 0.5 A49 22 b2 16 2 0 0 1 0 0 0 0 0 17 0.3 B49 0 61 0 2 0 0 23 3 0 1 0 0 10 0.03 C49 16 27 0 0 1 1 7 7 0 0 1 0 40 0.0? D49 1 + 64 1 0 2 0 1 0 0 0 0 0 28 0.1 E49 27 14 39 9 2 0 0 1 0 0 0 0 8 1.4 F49 1+6 29 6 0 1 0 0 0 0 1 0 0 17 0.06 G49 60 15 4 1 0 4 1 1 0 1 1 0 12 0.9 H49 68 24 2 0 0 4 0 0 0 1 0 0 1 0.9 149 18 15 11 13 2 1 0 0 0 3 0 0 37 0.6 A51 31 57 5 0 1 0 0 0 0 2 0 0 4 0.9 B51 0 53 7 2 28 0 0 0 0 2 0 0 8 3.0 C51 33 47 1 1 0 0 0 0 0 2 1 0 15 1.0 D5l 26 9 27 11 0 0 0 0 0 2 0 0 25 1.5 E51 18 23* 0 0 41 1 1 0 0 4 0 0 12 0.08 F51 23 53* 1 0 11 2 1 0 0 1 0 0 8 1.5 G5l 25 3^ 1 0 0 1 5 1 1 1 0 0 31 0.3 H51 49 24 4 1 0 0 0 0 0 3 0 0 19 1.1 151 13 6 30 3 11 0 0 0 0 11 0 0 26 0.7 A53 9 72. 6 9 12 0 0 0 0 1 0 0 0 5.8 B53 6 94 0 0 0 0 0 0 0 0 0 0 0 1.5 C53 10 3 4 9 0 0 0 0 4 1 0 24 0.3 D53 5 67* 1 1 23 0 0 0 0 3 0 0 0 16.2 E53 6 45 7 3 26 0 0 0 0 0 0 0 13 1.0 tJ 1 •H "S O O EH S a o a H 0 3 Q* m H s 0 1 < D S a •p 0 EH 0 3 01 03 (U < O EH M <4 O a o H a a a o a a co j - U \J - C M ONOMTvJ- C V JJ- O H C O lA O lT v O O • • • • • • • • • • • • • • • • • O O H O C M H O O O O H H H O O C v l H C M O O O O O O O O O O O O J* H rH (NCOCOJ- O J - J - J - C O . _ CO COHJ- COcOH CTsH CM UMTV 00 cO(Nlr\J-vO H J" O O O O O O O O O O O O O • • • • • • • • • • • • • O O CNCMrvcOCO O cOtNoO O Q — ‘ ‘ ' 0-00 OvJ- J-VO coco OvO O vO (NOCM OvOvCOvO H O OCM C M O O O M r\lr\H O J * O OCM C M O H C O C M O O COcOH O O CM J- H H C M C M C M H CM H C M H H H H H H O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O H H O O O O O O O c O C M H H O O H O O O c O j-C X 3 H jtU % v O I N H c O C M c O j-U v t J-J-cOud-CMCMU\HJ-COCMvO H H C M H H H C M H H O O O O O O O O O O O H C M H H C M COCOCM-4- H H O C'-vO HCO C M COH J * COCOCM J - H C M COH U\CM H C M C M C M O O O O O O O O O ^ O H O H O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O J ’ H O O O H O C M H J * H COcOfc\d*vO C M COH H cOcOCM J * CVlUMNj-vO COH H vO lr\CM COH J - CM M MrvCM H C O C M COO J * C M O J-V O OvH-d* C0ud-VfvcoJ- O INlr\OvCM lr\cOO„d-vQ cOcOcOJ* O O^CMJ- H H C O OvO J " J * CM COvO IrsCM H H H H H O O O O O O O O H O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O O CMOOOVOOOOCOO Cv-lfvvO CMUnO O O O O O O O O O O O O O O O O O O O O O O O O O O O O O C M C M H C M O O vO O O C M O O O O C M C V IU vO O OvO INUvoo C O C M C M H l c j - J - H C M J - U \ 4 - CM vO H vO COJ* C O IN O cOvO tNOVro H H H H C M C M J* C M j " H H C M C M C M C M H H C M H c p j - O vQ H O O OMNvO O O O J * COCOH C M H vO H COOvOVH tNCOvO C M COH ^ H cOud- vO COCOMmcm C M H H -d* COIN H J- J - IN C M CO C M CO O O v CO C M Uv CO C M C O C M INcOvO CM OOvO INCO Q IN H H J " O vC v-O .d'IrvrO J- O V C M C M CO CMvOvO O C M J - IN - COCO C M H J " cotNCM C O C M C M C M ^vcoJ*-d" j - j h - d - J* -d* J"vO Un vOCO C M C v-J* v O co^ ncO ^ v v O \r\4 - UMrv HvQvO INCM coCJvvOvO O OvlfsvO O H O trvvO C O C M 00 IfNvO vOCO OvO cOCNO-d" C M O C M OcOVO COvO C M C M J * J * J * cOCVJvOOO C M CO c i d H C M COH vrv C M COH CO H H H H H H H H H H H CM H < D F h h a) s | c d 3 caa ro CO co COMMrvlfvUMrvCv. t > - C v - I N - C v . C v . r lrv\r\\fMfvXfMr\\iN\fMrv\fvMMfv\r\lfv\rv« aoaH«s5pqoQa«daop m a t O H CO M “ \vO OcOVO Cv.00 V O IN OVQ J - COvO OVrOvO CMj-lfNCO CMJ* IINCO C T V rH r — IHHr-jCMCMCMCMCM CO CO COJr 3 ' UvUvlTNvO vO N-IN IN IN C O C O 137 I I HEAVY MINERAL FREQUENCIES IN PERCENT (Continued) Sample Number M i n e r a l s EP OP AM PX BI CH GA ZI TO AP SP ST Ot i H T712 23 37 3 11 0 0 13 1 0 0 9 0 3 0.3 T713 T714 27 3b s 1 2 7 11 0 0 0 0 7 3 0 0 0 0 0 0 18 7 0 0 3 2 0.3 0.3 T715 31 12 0 4 0 0 10 1 0 0 9 0 32 4 - 0.3 T723 T72*f 31 31 6 3 2 12 5 0 0 0 0 5 1 1 0 0 0 0 0 8 10 0 0 0.3 0.3 1714.7 29 32 1 11 0 0 0 0 0 12 0 2 0.3 T801 38 27 0 6 0 0 4 3 0 0 17 0 5 0.3 T811 31 36 0 1 0 0 6 6 0 0 15 0 5 0.3 T936 12 74- 0 0 0 0 3 2 0 0 8 0 1 T966 44 28 0 0 0 0 3 18 0 0 3 0 4 - T993 T99M- 27 4-3 1 0 0 0 8 7 0 0 10 0 4 - 15 65 0 2 0 0 7 3 0 0 6 0 2 T99- 27 4-2 0 0 0 0 5 4 0 0 x7 0 5 T996 23 35 0 0 0 0 4 12 0 0 2b 0 2 T997 29 37 0 0 0 0 5 8 0 0 19 0 2 T1001 43 32 0 0 0 0 2 4 - 0 0 15 0 4 - T1005 26 48 1 1 0 0 4 5 0 0 12 0 3 T1006 16 55 0 0 0 0 3 11 0 0 12 0 3 T1007 36 28 1 14 0 0 5 0 0 0 12 0 b LAI 28 44 - 28 - M - — - - - — 7.0 LA2 33 17 33 - 17 6.0 LA3 12 5 55 — 28 4. 7# 18.0 LA4 — 1 33 16 0 0 - - - 3 - 30.0 LA5 — 3 16 81 — - - — - - 0 - 0 32.0 LA6 mm 5 13 72 10 0 - 0 31.0 LA7 — 5 74 17 8? 1 - - am am 0 mm 0 41.0 LA8 — - 16 - - — — - am — — 6.0 LA 9 - 13 13 13 67 8.0 LAIO - 25 25 - 50 - mm - - - - - - 4-.0 LA11 20 10 20 0 30 10.0 LA12 20 10 10 0 60 35# 10.0 LA13 — 10 - 55 — — - — — — — — 31.0 LA14- - 6 14 6 7b 7.0 LAI 5 10 10 20 0 30 LA16 8 12 28 13 39 12# 9.0 LA17 - 4 34- 4-6 4 3^.0 BM3 0 72 0 28 2.3 bmh- 0 75 0 25 1.7 BM5 0 90 0 10 2.9 BM6 0 67 0 30 - - - - - am 3 - - 5.5 BM7 0 82 0 18 2.0 BM8 0 75 0 25 - 1.9 138 HEAVY MINERAL FREQUENCIES IN PERCENT (Continued) Sample Number M j L n e r a 1 s EP OP AM PX BI CH GA ZI TO AP SP ST ot % H GI1 50 20 5 5 mm 2 5 0 0 0 0 DAI 25 15 5 5 30 15 - mm 0 0 0 0 - DA2 25 15 5 5 30 15 - - 0 0 0 0 - DA3 25 15 . 5 5 30 15 mm - 0 0 0 0 - ST1 5 15 *5 0 25 ■M 0 mm 0 - 0 0 - ST2 5 20 5 30 0 0 0 0 0 - 0 0 mm ST3 20 20 30 0 0 5 0 0 0 0 0 0 - ST4 13 20 18 15 0 3 0 0 0 - 0 0 - 3A HG15 10 10 25 - 10 10 - - 10 - - HG16 _ 10 25 - - - - 10 - - 10 10 - 12.1 HG18 — 10 10 _ 25 - — 10 - - 10 - - 11.1 HG19 10 25 25 5 10 - 5 - - - - - - 0.5 EMI EM2 3 13 10 11 11 3 2 2 0 1 2 1 2 0 0 0 0 1 0 1 10 0 0 6 3 , 6 9.2 3.^ EM3 7 12 63 1 1 1 1 0 0 1 9 0 4 2.8 EM4 2 27 0 57 2 2 1 0 0 3 0 2 EM5 31 27 0 0 3 15 3 1 0 0 6 0 14 EM6 36 l*f 1 0 0 0 3 4 0 0 13 0 30 EM7 10 22 10 0 11 20 1 3 0 1 11 0 11 EM8 7 7 44 0 18 0 6 1 0 0 8 0 9 EM9 12 38 0 0 17 20 1 0 0 0 1 0 11 EM10 0 35 1 0 3 1 0 0 0 0 0 0 60 EM11 0 23 0 0 6 2 5 4 0 2 0 0 EMI 2 2 14 17 1 27 20 l 2 0 0 0 0 6 EM13 1 14 3 0 36 19 0 0 0 0 0 0 27 EM14 8 24 8 0 8 7 0 0 0 0 4 0 - EMI 5 26 21 4 0 5 12 2 3 0 0 10 0 APPENDIX D AVERAGE FREQUENCIES APPENDIX D AVERAGE FREQUENCIES Province Number ZI GA BI AP OP ST CH.EP TO AM SP PX OL % H 1. Rock OutcroDS and Rivers I 6 b 7 0 39 0 3 26 0 1 13 1 0 II 2 3 3 1 b6 0 0 2b 0 5 3 5 0 3.5 III 1 1 11 0 25 0 2 23 0 17 0 0 0 hi IV 1 1 15 0 20 0 1 6 0 25 2 19 2 if.8 Total 3 2 9 0 33 0 2 20 0 12 5 8 1 3.3 2. Beaches I 1 b 3 o 37 3 5 29 1 + 1 3 0 0 0.2 II 1 2 7 1 33 1 6 28 1 7 3 3 0 3.1 III 0 1 3 1 27 1 11 20 0 18 1 11 0 2.8 IV 1 1 12 1 9 1 10 7 1 35 1 10 0 6.8 Total 1 2 6 2 26 2 8 21 2 15 2 6 0 3.2 3. Inshore to 50 Fathoms I 2 3 lb 6 22 0 3 2b 0 2 2 1 0 1.2 II 1 1 5 3 2b 0 6 26 1 8 1 5 0 1.5 III 0 1 lb b 10 0 £ 16 1 Ilf 1 5 0 3.8 IV 0 0 6 2 8 0 b 6 2 32 1 8 0 6.i f Total 1 1 10 b 16 0 b 18 1 Ilf 1 5 0 3.2 Offshore oast 50 Fathoms I 1 2 5 1 32 0 1 1+2 0 2 1 1 0 1.0 II 0 0 9 3 3 5 0 1 27 0 6 0 2 0 2.1+ III 0 1 3 2 25 0 0 20 0 12 1 12 0 1.7 IV 0 1 6 6 9 0 l 10 0 i f 7 1 2 0 1.8 Total 0 1 6 3 25 0 l 25 0 17 1 I f 0 1.7 5. All Environments I 3 3 7 3 33 1 3 30 1 2 5 1 0 0.8 II 1 2 6 2 3b 0 3 26 1 7 2 I f 0 2.6 III 0 1 8 2 22 0 b 20 0 16 0 8 0 2.5 IV 1 1 10 2 12 0 b 7 1 35 1 10 1 5.0 Total 1 2 8 2 25 0 b 21 1 15 2 6 0 2.7 iVi AVERAGE FREQUENCIES (Continued) ZI GA BI AP OP ST CH EP TO AM SP PX OL % H 6. All Environment Based on 0.8^ Heavy Minerals I 3 3 7 3 33 1 3 30 1 2 5 1 0 1.0 II 3 7 20 7 111 0 10 85 3 23 7 13 0 3.3 III 0 3 25 6 69 0 12 62 50 50 3 2 5 0 3.1 IV 6 6 63 13 75 0 25 Mf 26 219 66 63 6 6.3 APPENDIX MAPS M A P I HEAVY MINERAL PROVINCES IN SOUTHERN CALIFORNIA MAP I HEAVY N map a i r P R O V I N IN SOI o P R O V I N C E i A SIN S A N MIGUEL I H 4 3 ! SA N T A R O S A / PRO V MONICA S IN B 4 5 =^ V S A N 7 A C R U Z \ B A S I N SA N T A R O SA ~ C O R T E S RID G E ATALINA I C A T A L IN A B A S I N S A N N IC O L A S B A S IN W " \ >.G4 C L E M E N T E I. I ' ' B A N K A LO NG HEAVY MINERAL PR O V IN C ES IN S O U T H E R N CALIFORNIA 59_____ ->o a o P R O V I N H 4 3 ! A M PH IB O L E WATER DIVIDE " PR O V IN C E B O R D ER « P R O V IN C MONICA S I N I C R U Z V A S IN p A N 7 i v $ M R B A R A 7. A TA LIN A / C A T A L IN A B A S I N S A N S A N N IC O L A S B A S IN W " C L E M E N T E I. I s I C O R T E S B A N K U .S..A .. - 'MEXICO ft «\ \ \ E M I 4 R O U G H E C O R T E S B A SIN p . * V C O R T E S -> 1 _ _ X B A S I N PROVINCE V MAP II HEAVY MINERALS ASSEMBLAGES SURF TO SANTA BARBARA SURF TO SANTA BARBARA HEAVY MINERAL ASSEMBLAGES OTHER- ^ --- EPIDOT E — OPAQUE PYROXENE• _____ -AMPHIBOLE R __________________ RIVER •••••__,___ WATER OIVIOE 0 2 4__ 6______8 r~ — -T -T M ----------1 STATUTE MILES 'SURF T I0 0 5 PT.ARGUELLO -I- 30 ' 207 10* HEAVY MINERAL ASSEMBLAGES SANTA BARBARA TO POINT DOME 40' 3 0 '.......... 30' ■ ' I 1 1 " o «?■ ••• , g R ^-T-J2 5 c/<s r-s * t8 . i 20 I o ' 34° ' Q , Q TBOl Q “7 B27 D4I © 20' ■ ■ i DAI DA 2 S.AN^ DA 3 HAIO HAI3 HAI5 B 39 OiO C£»C£ OvCu Q E45 © H 43 40* 30' 20' m a p in 20' 10* 119- 50' SANTA BARBARA TO PT. DUME x.... / HEAVY MINERAL ASSEMBLAGES OTHER_______________ ___— EPIOOTE OPAQUE - AMPHI0OLE R _________________ RIVER PYROXENE WATER DIVIDE J f JURASSIC FRANCISCAN Os 0LI60CENE S ESPE + 30 * 20' STATUTE MILES haio HA 13 HAI5 HA 2 7 OtO Q HA 36 \ A 15 HA39 DUME uUMt CANYON MAP IV HEAVY MINERAL ASSEMBLAGES POINT DUME TO CORONA DEL MAR / IO' 34 50 40 J-A. S C55 A 4 9 m & C 4 5 HA65 SANTA MONICA E7 HA74 R fTHOM Sr'O DUME CANYON PT.DUME TO CORONA DEL MAR HEAVY MINERAL ASSEMBLAGES C 3 / 0*0° n C A 0 ' * OTHER PYROXENE EPIOOTE - OPAQUE AMPHIBOLE R -----------------------------------RIVER _________ WATER DIVIDE PI----------------i — PLEISTOCENE P L s— SAN PEDRO SAND “ P u UPPER PLIOCENE P r REPETTO " M ____ MIOCENE M m MODELO " Ml TOPANGA “ O* OLIGOCENE SESPE PAm — PALEOCENE MARTINEZ J p JURASSIC PLUTONIC J d “ DIKE J m “ METAMORPHIC / / / E 4 9 PALOS VERDES HILLS / / I 2 ' - TT STATUTE MILES map nr 20' — i — ' .T B 49' Mt A 49| M 1 0 ' —r~ , o , - •Iff ue* 50 ' ! s T r J p ST21 Jd ST 3 J m 1 0 ' C 4 9, Mm C 4 5 Pu PL 0 4 5 ^ .C ll R HA74 R 34 " <*/<2r PALOS VERDES HILLS :~fi3 CORONA NEWPORT CANYON 40* HEAVY MINERAL ASSEMBLAGES EL MORRO TO SOLANA 30' 20' EL MORRO !VBI3 AI3 OTHER PYROXENE 0 1 0 ' R _____________________ RIVER •......... WATER DIVIDE P L t _ PLEISTOCENE TERRACE Mm_____MIOCENE MONTEREY M s-------- " SAN ONOFRE SAND M v " VAQUEROS E s EOCENE SANTIAGO PAs PALEOCENE SILVERADO T v_____ TERTIARY VOLCANIC K «_____ CRETACEOUS WILLIAMS Kp " PLUTONIC J p JURASSIC PLUTONIC ■Rm____ TRIASSIC METAMORPHIC 2 I 4 r - STATUTE MILES LA 13 H 45 • SAN CLEMENTE H II U J ( L U V D 35 cn.cr \ DI7 A 3 5 H 33 \ EL MORRO TO SOLANA HEAVY MINERAL ASSEMBLAGES EPIDOTE OPAQUE AMPHIBOLE 1 15 (m 30’ 1 — iLA 14 _ + * ■ ■j'1 . / i ^ N K p / v_y-t^7 I 1*<t< 20' + r°*E n •-/ / / / .-■■ / .•■ / / / / / /•' MTS. IO1 + C * # * * - L A 7 Kp 40* jj i H 4 5 * Kw / I I I I L U O LA 13 LA 6 LA 3 ' h \ 30' LA 2 «*£ **<»► . Jp ( o cn Q_ G I 71 LOUIS 1*1 - -f- 20' l s N « 's I ' I I \ I \ » S ' - "^O/OHD* L A 4 LA 5 LAII IO* , K P / r ( RIVER LA II Kp cV a' / BM4 Tw IO^ 1 1 7 * 33* MAP VI HEAVY MINERAL ASSEMBLAGES SOLANA TO MEXICO CANYON "ISQUITOS EM 15 E 3 3 JOLL EM 8 Pd BM 7 15 BM 3 HG (6 HG 19 Pz SAN DIEGO PT. LOMA G 2 2 H 2 2 r \.y HG P Ps EMI2 0 U S^ 4 : . - MEXIC O HG SOLA HEAVY COHONAOO can*?n -- L - OTHER ~" PYROXENE - I AMP U 20* Es EM 14 4 * I O' R ____________________ RIVI WATER DIVII P s _______PLIOCENE SAt Pz " / SWEITZE P d “ SAN DIEG E s EOCENE SAND _________ I ______ 117 • I o' 117 * 7 * 7 L A S Kp • 50* MAP3EE 33 QUl T p S _ S A N Y O a/^ syuj BM 6 Td m BM 5 Td LA 9 Kp ,C > V J f S / -V?- BMS Tv / / f / / f t / / JKp LA*« / LA 17 50 0, 6 ' 0» HG IS HG 19 BM 3 Tv BM 7 Tv A?' LA 16 LA 17 SAN DIEGO aV ' r \ \ \ O T A r t.p- $AN LA 16 LA 17 y.?jDR( ^ MtSA O'............. • HG IB Ps ULS^A^ _ MEXICO O ' SO LA N A TO MEXICO HEAVY MINERAL A SS E M B L A G E S 40 30' OTHER ~ - PYROXENE - EPIDOTE - OPAQUE AMPHIBOLE P s ___ P z _ . P d __ E s __ O' _________________RIVER WATER DIVIDE PLIO C E N E SANDSTONE " / SWEITZER “ SAN DIEGO EOCENE SANDSTONE _____ I _____________ 117 ° T d ___________ TERTIARY DIKE T v ______________ " VOLCANIC Kp CRETACEOUS PLUTONIC K ___________ CR ETA C EO U S J K p _ JURASSIC a n d K PLU TO N IC 0 2 4 6 r" - n i 1 STATUTE MILES 50

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Creator Azmon, Emanuel (author)

Core Title Heavy Minerals In Sediments Of Southern California

Degree Doctor of Philosophy

Degree Program Geology

Publisher University of Southern California (original), University of Southern California. Libraries (digital)

Tag Geology,OAI-PMH Harvest

Language English

Contributor Digitized by ProQuest (provenance)

Advisor Emery, Kenneth O. (committee chair), Bandy, Orville L. (committee member), Clements, Thomas (committee member), Merriam, Richard (committee member), Reith, John W. (committee member)

Permanent Link (DOI) https://doi.org/10.25549/usctheses-c18-74749

Unique identifier UC11357416

Identifier 6004473.pdf (filename),usctheses-c18-74749 (legacy record id)

Legacy Identifier 6004473.pdf

Dmrecord 74749

Document Type Dissertation

Rights Azmon, Emanuel

Type texts

Source University of Southern California (contributing entity), University of Southern California Dissertations and Theses (collection)

Access Conditions The author retains rights to his/her dissertation, thesis or other graduate work according to U.S. copyright law. Electronic access is being provided by the USC Libraries in agreement with the au...

Repository Name University of Southern California Digital Library

Repository Location USC Digital Library, University of Southern California, University Park Campus, Los Angeles, California 90089, USA