University of Southern California Dissertations and Theses

Paleocurrent analysis of the Upper Cretaceous, Paleocene and Eocene strata, Santa Ana Mountains, California

(USC Thesis Other)

Paleocurrent analysis of the Upper Cretaceous, Paleocene and Eocene strata, Santa Ana Mountains, California

PDF

Download a page range

Download transcript

Copy asset link

Request this asset

Transcript (if available)

Content PALEOCURRENT ANALYSIS O F THE UPPER CRETACEOUS, PALEOCENE AND EO CENE STRATA, SANTA ANA MOUNTAINS, CALIFORNIA by Robert Allen Davis, Jr. A Thesis Presented to the FACULTY O F THE GRADUATE SCHOO L UNIVERSITY OF SOUTHERN CALIFORNIA In Partial Fulfillm ent of the Requirements of the Degree MASTER OF SCIENCE (Geological Sciences) June 1978 UMI Number: EP58638 All rights reserved INFORMATION TO ALL USERS The quality of this reproduction is dependent upon the quality of the copy submitted. In the unlikely event that the author did not send a complete manuscript and there are missing pages, these will be noted. Also, if material had to be removed, a note will indicate the deletion. Dissertation F H jfe lis W n g UMI EP58638 Published by ProQuest LLC (2014). Copyright in the Dissertation held by the Author. Microform Edition © ProQuest LLC. All rights reserved. This work is protected against unauthorized copying under Title 17, United States Code ProQuest LLC. 789 East Eisenhower Parkway P.O. Box 1346 Ann Arbor, Ml 48106- 1346 UNIVERSITY OF SOUTHERN CALIFORNIA TH E GRAD UA TE SCHO O L U N IV E R S IT Y PARK LOS A N G E LE S, C A L IF O R N IA 9 0 0 0 7 G e D This thesis, written by Robert Allen Davis, Jr. under the direction of h.A^...Thesis Committee, and approved by a ll its members, has been pre sented to and accepted by the Dean of The Graduate School, in partial fulfillm ent of the requirements fo r the degree of Master Science - Geological Sciences Dean D ate Ï-A Î.:2K .. THESIS COMMITTEE Chatrman. é J . CONTENTS ABSTRACT ........................................................................... INTRODUCTION . . . . . . .-................................. Purpose ..................................................................... Locality and Accessibility ......................... Methods ..................................................................... Computer Programs ............................................ Regional Setting .................................................. Acknowledgements .................................................. STRATIGRAPHY ..................................................................... Cretaceous System ............................................ Upper Cretaceous Series ......................... Ladd Formation ............................... Baker Canyon Member . Holz Shale Member Williams Formation . Schulz Ranch Member . Pleasants Sandstone Member Tertiary System ............................................ Pal eocene S e r i e s ..................................... Page V 1 1 2 5 6 8 11 12 12 12 12 12 15 16 16 17 18 18 n Silverado Formation Eocene Series . . . Santiago Formation PALEOCURRENT RESULTS . . . . PALEOGEOGRAPHIC IMPLICATIONS . , CONCLUSIONS ............................................ REFERENCES . APPENDICES . Appendix 1 Appendix 2 Appendix 3 Appendix 4 S tatistical data showing paleocurrent directions by class frequency, vector and arithmetic mean, consistency ratio and vector magnitude. Each division on the rose diagram equals one data value, unless noted otherwise . Paleocurrent measurements, listed by formation and lo c a lity . Primary sedi mentary structures are identified. . Computer program for rotation (two- t i l t ) ............................................................... Page 18 19 19 21 » # 3% Vector mean program and input instruc tions ............................................................... n m 72 111 ILLUSTRATIONS Figure Page 1. Location m ap showing study area and local geographic features ................................................................................. 3 2. Geologic map of the study area with sample locations as given in Appendix 1 (a fte r California Division of Mines and Geology, 1 9 6 6 )..................................................... 9 3. Columnar section of the Upper Cretaceous to Eocene strata, Santa Ana Mountains, California (a fter Roth, 1 9 5 8 ) ........................................................................................ 13 4. Geologic m ap with rose diagrams showing paleocurrent directions for the Holz Shale, Upper Cretaceous Series. See Appendix 2 for d a t a .................................... 22 5. Geologic m ap with rose diagrams showing paleocurrent directions for the Schulz Ranch Member, Upper Creta ceous Series. See Appendix 2 for data . . . . >24 6. Geologic map with rose diagrams showing paleocurrent directions for the Pal eocene Series. See Appendix 2 for data . .. . . . . . 26 7. Geologic m ap with rose diagrams showing paleocurrent directions for the Eocene Series. See Appendix 2 for d a t a .................................................................................. IV ABSTRACT Paleocurrent data and primary sedimentary structures have been used to interpret sediment transport directions and depositional environments from the Upper Cretaceous to Eocene sedimentary strata in the Santa Ana Mountains, Orange, Riverside and Sam Diego Counties, Cali fornia. A total of 241 measurements, predominantly cross-bedding, were recorded. A vector mean computer program was u tilized to compute the resultant vector direction. The paleocurrent study of the Upper Cretaceous strata shows the development of a marine basin of deposition. A gradual encroachment of the sea or subsidence of the terrane during the deposition of the Ladd Formation brought water depths to outer shelf to bathyal. These sediments are represented by a distal tu r- bidite facies. At the close of Cretaceous time the seas retreated and deposition of the Williams Formation took place in near-shore shallow marine environments. Pal eocene sediments of the Silverado Formation indicate a transport direction from the southeast. During this time sedimentation occurred in marginal marine to onshore environ ments. Near-shore marginal marine sediments of the Santiago Formation typify Eocene strata and a west-northwest direction of sediment trans port is indicated from paleocurrent data. y_j INTRODUCTION Purpose This study was undertaken to determine the direction of sediment transport and to relate these data to depositional environ ments and to the paleogeography of Upper Cretaceous to Middle Eocene sedimentary rocks in the Santa Ana Mountains, Orange, Riverside and San Diego Counties, California. This was accomplished by measuring paleocurrent directional indicators in primary sedimentary structures and the subsequent s ta tis tica l analysis of these data. The f ir s t comprehensive study of the Santa Ana Mountains was undertaken by Popenoe (1936) in which he described and extensively mapped the Upper Cretaceous rocks and faunas of the area. Popenoe and Woodring (1945) published a report on Paleocene and Eocene s tr a ti graphy in the northern Santa Ana Mountains. Stevenson (1948) subse quently reported on the stratigraphy of the southern Santa Ana Moun tains. Roth (1958) compiled a comprehensive report concerning the geology of the southern Santa Ana Mountains. There have been numerous hypotheses formed concerning the paleogeography and structural evolution in southern California and its adjacent borderland. One of the earliest and most comprehensive reports on the structural evolution of southern California was by Reed and H ollister (1936). More recent work on structural relation ships and paleogeography have been compiled by Yerkes and others (1965), Yeats (1968), Woodford and others (1972), and Yeats and others (1974). The Paleocene geography of the southern California area has been discussed by Sage (1973a and 1973b). Work on the middle Eocene paleogeography was presented by Howell (1975) and Howell and others (1974). There has been much written concerning the paleoenvironment interpretation of sedimentary structures. Reports useful for this study include Tanner (1955), Allen (1963), Dott (1963), Klein (1967) and Stauffer (1967), Middleton and Hampton (1973), Walker and Mutti (1973) and Link (1975). Locality and Accessibility The area of this study is approximately 64 km southeast of the city of Los Angeles and encompasses 380 km (Fig. 1). The majority of the fie ld area is in Orange County with segments of San Diego and Riverside counties included. Field measurements were taken during the months of June, July and August, 1974. Additional data were collected during June, 1975. The following United States Geological Survey 7.5-minute series quadrangles were used in the study: Orange, Black Star Canyon, Corona South, Tustin, El Toro, Santiago Peak, and Canada Gobernadora. Observations were hindered by heavy brush and rough topography. Fire Figure 1. Location map showing study area and local geographic features. ï- < \» g//— 11 C O -I O U J _ie> roads and breaks provided excellent, although lim ited, access to the study area. Much of the land is privately owned and permits are re quired to gain entry. During the summer months special fire permits are also necessary as this is a high fir e danger area and is under the control of the National Forest Service. Methods Measurement of sedimentary features were made with the Brunton compass and level board following the methods set forth by Compton (1967), and Pettijohn and Potter (1963). Only the most clearly defined sedimentary structures were measured in order to mini mize the possibility of error. In the measurement of cross-bedding orientation the sedimentary structures were excavated to obtain a three-dimensional view. This made i t possible to record the true dip and dip azimuth, rather than dip components. The most widely recognized feature described in this report is cross-bedding which has been defined as "a structure confined to a single sedimentation unit consisting of internal bedding, called fore set bedding, inclined to the principal surface of accumulation" (Potter and Pettijohn, 1963, p. 69). The most commonly observed type of cross-bedding in the study area is trough tangential form. Trough planar and tabular tangential cross-bedding was observed but on a limited basis. Only one measurement per one cross-bedding set was recorded in the s ta tis tic a l analysis. In sets where several data values were observed, an average reading was calculated to eliminate any possi b ility of one set of cross-bedding having a larger weight than any other set. Measurements were corrected for regional dip. Other features which were observed included bounce casts, parting lineation, scour channels, oriented fossils, and pebble imbri cation. Oriented fossils, in this instance T u rite lla , were measured and analysed according to the procedure described by Merschat (1971). Computer Programs Two computer programs were used in the analysis of the paleo current directions. The vector mean computer program was u tilized to compute the resultant vector direction and the rotation program was used to correct the data affected by regional tilt in g . Sedimentary structures are among the most widely used c r i te ria in the evaluation of depositional environments. Reliable in te r pretation of these data can be achieved through the proper use of s ta tis tic a l analysis. One of the d iffic u ltie s in the analysis of orientated data is the problem of selecting an origin in order to divide a circular distribution into a linear frequency curve. Jizba (1953) and Chayes (1954) observed that there w ill be a significant difference in the mean and variance calculations when there is a change in the choice of origin of one class interval or perhaps even a few degrees. They indicate that most geologic applications, where no point of origin can be determined, the mean w ill not be a good indication of preferred orientation direction and that the variance win be questionable in determining the significance of the d is tr i bution, Chayes (1954) proposed a vector method to analyse orienta tion data which avoids the problems of selecting an origin. This is possible because the use of descriptive statistics for preferred orientation direction and dispersion are independent of origin. In this vector summation method, each data point is considered a vector with magnitude and direction. In this study the magnitude was assumed to be unity. The north-south and east-west directional components were computed by multiplying the magnitude by the cosine and the sine of the azimuth, respectively. These directional components are then sum m ed to give a resultant vector which also has the components of direction and magnitude. The resultant vector, R, therefore, is equal to [(sine)^ + (cos)^]'^, and would be a measure of the dispersion of the observed vectors. The resultant vector with no dispersion would have a magni tude equal to the total number of observed vectors those with dispersion would have a value somewhat less than (n). Vector magnitude presents two problems: 1) I t differs with the groupings of observed vectors, and 2) i t changes in magnitude with the number of observed data. Curray (1956) introduced a consistency ra tio , L, to alleviate this problem. "L" is calculated by dividing the vector magnitude (R) by the number of observed data (n) and then mul tiplying by 100: thus L = R/n x 100. By use of this consistency ra tio , the grouping of data with no dispersion would equal 100; whereas, those groupings which exhibited a great deal of dispersion would approach 0. By using Curray's consistency ra tio , vector magnitude can be a useful and sensi tive measure of dispersion. The vector summation computer program used in this study, based on Curray (1956), was written by Charles Barker and data were processed on an IBM 371-65 computer. The "Tw o-tilt problem computation" program was obtained from the Union Oil Company of California's Research Division, Brea, C alifor nia. The standard techniques of restoring a structure to its original position before deformation have been described by Donn and Shimer (1958) and Fisher (1938). Regional Setting The Santa Ana Mountains consist of a series of rocks ranging in age from Jurassic-Triassic through Pleistocene. Structurally, the area is regarded as a tilte d fa u lt block with a structural trend of northwest-southeast (Roth, 1958). Strata exhibit a gentle westerly dip and are separated from the fla t-ly in g sediments of the Perris block to the east by the Elsinore Fault System (Fig. 2). Basement rocks in the area studied have been described by Allison (1970) and separated into three groups: andesitic volcanics, intrusive granodioritic rocks and prebatholithic sandstone and a r g illite . The basement complex in the Santa Ana Mountains is ' Jurassic-Triassic in age (Allison, 1970). 8 Figure 2. Geologic m ap of the study area with sample locations as given in Appendix 1 (a fte r California Division of Nines and Geology, 1966). P u H Corona Ep JTr, Ku , 2 5 24 JTr, Ju • 8 Sonfo Ana JTr, ^ 2 2 J T r, ,EP Ju JTr, Pu Ku JU Pu Ju Pu J T r, Ku 28 P A C IF IC ' OCEAN Ku Quaternary deposits - undifferentiated Upper Pliocene marine Miocene deposits - undifferentiated Oligocene - undifferentiated Eocene marine Pal eocene - undifferentiated K u Ju Jtrv g r bi Upper Cretaceous - undifferentiated Upper Jurassic - marine Jura - trias metavolcanic rocks Mesozoic granitic rocks Mesozoic basic intrusive rocks 10 Acknow!edgements My appreciation is extended to the Union Oil Company of California which sponsored this project, in particular A. A. Almgren, G. C. Brown, T. R. Redin and J. Friberg. Charles Barker was invaluable as a fie ld assistant. Permission to enter private property was granted by the following corporations: Casa de Coto Corp., the Irvine Company and the Rancho Mission Viejo Company. Appreciation is expressed to J. M. Evensen and S. L. Knight for their enduring encouragement. Dr. R. H. Osborne served as research advisor and Drs. D. S. Gorsline and R. 0. Stone served on the thesis committee. 11 STRATIGRAPHY The stratigraphy of the Upper Cretaceous to Eocene sediments of the Santa Ana Mountains is summarized in Fig. 3. Upper Cretaceous Series: Ladd Formation The Ladd Formation was named by Popenoe (1936), who described the Upper Cretaceous strata. Its type lo cality is at the mouth of Ladd Canyon in Silverado Canyon. The formation has been divided into two members by Popenoe; the basal conglomerate and sandstone, named the Baker Canyon Member (Popenoe, 1942) and the Holz Shale Member, which consists mainly of siltstone. Baker Canyon Member The Baker Canyon Member consists of submergent (transgres- sive) marine conglomerate and sandstone. Its type lo c a lity in Baker Canyon exhibits excellent exposures forming steep c liffs . The gray, massive conglomerate contains volcanic, plutonic and metamorphic cobbles that are well rounded, averaging 10-12 cm in diameter. The conglomerate grades upward into a wel1-cemented, coarse-grained sand stone. Popenoe, and others (1960) assigned a middle to late Turonian age to the upper part of this member based on megafossil assemblages. Foraminifera have been identified in the upper siltstone beds but are not defin itive for age determination (Almgren, 1973). 12 Figure 3. Columnar section of the Upper Cretaceous to the Eocene sediments, Santa Ana Mountains, California (a fte r Roth, 1958). 13 < ( r L U L U h“ C O > C O C O L U C C L U en g s (r o L l. or L U 00 S L U C O > - C O o L U o z u k : o o X X h - 1 - u DESCRIPTION g o N G z L U O ü 8 O [S X < o r L U h - 0) D O L U O 0 L U 0: o LU z Ü J U O LU O O < h * Z < (0 L U Z L U C J O L U _ J 2 o Û 2 lU (/) U) 3 O ü J u g Ü J o : o C E (U 0_ 0_ D O) z J u Q O < _J P CO o z < CO X O Z < Q C N _l D X O (O s i o: z U j O il o o o o CJ O 0 CD C C J 1 O o o C O fO -og o m CJ — O o 00 Sandstone - white to yellow-gray, thick bedded, coarse-grained, arkosic sandstone, moderately indurated. Abundant cross s tra tific a tio n . Burrows com m on. Sandstone - buff-tan, fine to medium grained sandstone, well sorted and poorly indurated. Local lig n itic coal beds. Local gray-green shale lenses, occasional conglomeratic lenses. Abundant cross s t r a t if i cation. Sandstone - lig h t gray to buff, very fine-grained, micaceous, s ilty to shaly sandstone, interbedded with calcareous siltstone and sandy, limy concretions. Sandstone - red-brown to buff, unsorted poorly bedded, medium to course-grained, feldspathic sandstone. Occasional conglomeratic lenses. Conglomerate - red-brown, well sorted, poorly bedded, friable cobble conglomerate. Clasts are well rounded, fresh, composition of siliceous slate, chert, quartzites, plutonic and volcanic rocks. ■ Shale - Basal dark gray to buff-brown fine-grained, s ilty sandstone, grades to clayey siltstone to dark gray m ud stone. Poorly indurated, highly fractured, good fis s ility . Locally interbedded with conglomerate and sandstone lenses, occasional calcareous concretions. Sandstone and Conglomerate - brown-gray, massive conglomerate; volcanic, plutonic and metamorphic clasts. Conglomerate grades upward into gray-buff sandstone. . Well indurated and fossiliferous. 14 In a more recent study, Popenoe (1973) reported collecting shallow marine molluscs from this unit which indicate a major marine inundation during Turonian time. This study points to a major u p lift to the east of the Santa Ana Mountains. This is substahti%edY(;yC3:h& igneous and metamorphic nature of the conglomeratic clasts in the Baker Canyon Member, which indicate the presence of a basement complex to the east. Holz Shale Member Conformably overlying the Baker Canyon Member is a basal fine-grained s ilty sandstone unit which grades upward to a clayey siltstone and fin a lly to a dark gray mudstone. The type lo c a lity is described a fte r rocks exposed on the Holz Ranch in Silverado Canyon (Popenoe, 1936). The Holz Shale reaches a maximum thickness of 487 m (1500 feet) in the northern Santa Ana Mountains and thins to the south with a minimum thickness of approximately 65 m (200 f t ) . The transitional contact between the Baker Canyon Member and the overlying Holz Shale Member reflects a gradual deepening of the basin of deposition. The basal section of the member appears to be of shallow marine origin. Colburn (1970) reported that abundant, in situ shallow water molluscs are found in the basal sandstone units and that the megafossils are Turonian in age. There is a question of whether this sandstone belongs to the top of the Baker Canyon Member or the basal units of the Holz Shale Member. The middle units of the Holz Shale Member consist of thick 15 dark mudstone with lenses of sandstone. Foraminifera in these units are not d efin itive but Almgren (personal communication) feels that they are indicative of deep water. Distal tu rb idites appear to have been deposited on the basinal plains. In Black Star Canyon, a dia- m ictite facies was observed. Features identified include load casts, gradational bedding, sand channels, slump folds and m ud clasts. The gradational nature of the Holz Shale Member, the marine biot and previous studies (Almgren, 1973; Colburn, 1973) indicate a definite deepening of the basin beginning with the deposition of the Holz Shale Member. Except for the basal shallow water units, the sedi ments were deposited in an outer shelf to bathyal environment. Williams Formation The Williams Formation is the youngest Cretaceous unit in the Santa Ana Mountains. The ;type lo c a lity , described by Popenoe (1936), is near the mouth of Williams Canyon. The formation is sub divided by Popenoe into two members. The basal conglomerate and feldspathic sandstone was termed the Schulz Sandstone and Conglomerate Member and la te r renamed the Schulz Ranch Member (Woodring and Popenoe, 1945). The Pleasants Sandstone Member conformably overlies the Schulz Ranch Member and consists of a massive shaly-sandstone and siltstone. I Schulz Ranch Member i The Schulz Ranch Member has its type lo c a lity approximately j 1200 m upstream from the mouth of Williams Canyon. This member I 16 consists of a basal cobble conglomerate facies which fines upward and la te ra lly into a coarse-grained feldspathic sandstone facies. Locally, cobbles and boulders are interbedded with the sandstone. The. Schulz Ranch Member is topographically distinctive in that i t is more resis tive than surrounding rocks and forms distinctive c liffs . The basal conglomerate facies of the Schulz Ranch Member is a red-brown, well-sorted, poorly-bedded, friab le cobble conglomerate which is interbedded with unsorted, poorly-bedded, medium- to coarse grained feldspathic sandstone. The 1ithology of the cobbles ranges from metamorphic black siliceous slate, chert, and quartzites, pluton ic igneous rocks, and varieties of volcanic rocks. The base of this member lies unconformably on the Holz Shale Member. Almgren (1973) noted that the abrupt change from the bathyal mudstone of the Holz Shale Member to the shallow water sediments of the Schulz Ranch sequence supports the presence of the mapped unconformity. Pleasants Sandstone Member The Pleasants Sandstone Member conformably overlies the Schulz Ranch Member. The type lo c ality is described in the vic in ity of the Pleasants Ranch near the mouth of Williams Canyon and was iden tifie d by Popenoe (1936). The Pleasants Sandstone Member is discontin uous in its distribution throughout the Santa Ana Mountains due to faulting and extensive Tertiary overlap (Roth, 1958, and Stevenson, 1948). The Pleasants Sandstone Member consists of very fine-grained. 17 1ig h t-to -y e l1ow-gray micaeous, s ilty to shaly sandstone interbedded with calcareous siltstone and sandy, calcareous concretions. The sandstone is poorly indurated, and appears to have low porosity and permeabi1i t y . The most distinctive characteristic of the Pleasants Sand stone Member is the occurrence of limy siltstone and sandy limestone concretions. Popenoe (1936) used these features to determine the contact between the base of the Pleasants Sandstone Member and the top of the Schulz Ranch Member. The fine-grained nature of the rocks and the abundance of plant material indicate a moderately low-energy environment, probably originating in a shallow marine basin. Faunal assemblages described here include Metaplacenticeras eupachydiscus (Popenoe, 1973). Tertiary System Paleocene Series: Silverado Formation The Paleocene Silverado Formation was o rig inally assigned to the Eocene Martinez Formation by Dickerson (1914) and was later assigned to the Paleocene Formation and renamed "Silverado Formation" by Popenoe and Woodring (1945). This formation unconformably over lies the Upper Cretaceous Series. The type lo cality is approximately 1625 m north of Santiago Canyon and typically consists of yellow-gray, fine to medium-grained s ilty sandstone. Bio tite is abundant in this 18 quartzite sandstone. Locally, gray-green lenses of shale are present as are occasional conglomeratic lenses. The formation is well sorted and poorly indurated. Bedding ranges from thinly laminated to massive. The Silverado Formation exhibits excellent and abundant trough-tangen tia l cross-bedding and scour features. Som e pebble imbrication occurs in conglomeratic lenses. A distinctive feature of the Silverado Formation is the pre sence of lig n itic coal beds. Som e of these are voluminous enough to be mined, although only in limited quantity. The presence of lig n itic carbonaceous shales and pi soli tic sandy clay indicate an environment which was a restricted lagoon or perhaps lacustrine in nature. These sediments may have been deposited in a shallow marine bay, or perhaps in interdistributary bays within a deltaic complex. Eocene Series: Santiago Formation The name "Santiago Formation" was proposed by Popenoe and Woodring (1945) and its type lo cality is approximately 800 m north of Irvine Park. The Santiago Formation consists predominantly of a thick- bedded white -to-yellow-gray arkosic sandstone. Lenses of coarse grained sandstone, clay, shale and conglomerate occur locally. The bedding is massive with locally abundant trough tangential cross bedding and scour features. Shale rip-up clasts are com m on and 19 occasionally poorly defined loading features are found at sand-shale interfaces. V ertically oriented burrows are locally abundant. These are unlined, 1-3 cm wide, and 4-6 cm high. Wei 1-developed channels are exposed along the Ortega Highway at the southern end of Canada Gubernadora. Lenses of coarse-grained sand and pebbles indicate a possible tidal channel, storm surge chan nel or perhaps a flu vial system cutting a bar, although the existence of a bar is questionaBle because i t is pebbly and highly bioturbated. The sediments in some of these units were probably the result of rapid deposition, as evidenced by the abundant load features. These sediments accumulated in a nearshore-marginal marine environment, possibly in a flu vial or deltaic setting. 20 PALEOCURRENT RESULTS A total of 241 measurements of primary sedimentary features were collected in the fie ld . Cross-bedding accounted for 91 percent of these, or 220 data points. Twelve measurements were from the Upper Cretaceous Holz Shale (Fig. 4). These structures consisted of oriented T u rite lla shells observed in a coquina bed near the top of the member (see Fig. X) and gave a vector mean of 105 degrees, a standard deviation of 90 degrees with a consistency ratio of 39 percent. Measurement of 24 data points observed in the Schulz Member of the Williams Formation (Upper Cretaceous) (Fig. 5) indicated a transport direction of 194 degrees with a standard deviation of 103 degrees. High variance was indicated by a consistency ratio of 14 percent. Eighty-five data points were collected from the Silverado Formation (Fig. 6). A sediment transport direction of 335 degrees and a consistency ratio of 48.32 gave the best s ta tis tica l results. The standard deviation for the data is 73 degrees. The largest number of data points (120) were observed in the Eocene Santiago Formation (Fig. 7). The data revealed a vector mean of 286 degrees with a standard deviation of 90 degrees. Moderate variance was exhibited by a consistency ratio of 25 percent. 21 Figure 4. Geologic map with rose diagrams showing paleocurrent directions for the Holz Shale, Upper Cretaceous Series. See Appendix 2 fo r data. 22 118*45 Corona Sonfo Ana \ P A C IF IC O CE AN II8 04 S 23 Figure 5. Geologic m ap with rose diagrams showing paleocurrent directions for the Schulz Ranch Member, upper Cretaceous Series. See Appendix 2 for data. 24 II8®45' Corona Santa Ana \ P A C IF IC O CE AN 25 Figure 6. Geologic map with rose diagrams showing paleocurrent directions fo r the Pal eocene Series. See Appendix 2 for data. Santo \ P A C IF IC OCEAN 27 Figure 7. Geologic map with rose diagrams showing paleocurrent directions for the Eocene Series. See Appendix 2 for data. 28 Corona S3®45 Sonfo Ana 3 3 * 3 0 P A C IF IC O C E A N 1 1 6 *3 0 ' 29 PALEOGEOGRAPHIC IMPLICATIONS The Upper Cretaceous series marks the beginning of subsi dence and gradual deepening of the depositional basin. Vertical grada tion from the non-marine Trabuco conglomerate^to the near-shore mar ginal marine Baker Canyon conglomerates and sandstone suggests a grad ual inundation by the sea or possibly the subsidence of the terrane. The submergence continued with the deposition of the Holz Shale. The shallow-water biota in the Baker Canyon and early Holz Shale Members gave way to deeper-water foraminifera. Study of foraminifera indicates a depth range from outer shelf to bathyal (middle bathyal or deeper) (Almgren, 1973). Field observations suggesting a distal turb idite fa- I cies perhaps deposited on the outer fan seems compatible with the avail-| able paleontological evidence. The rose diagram for the Holz Shale M em ber is based on data from measurements of oriented T u rite lla displaced from shallower waters and does not imply an actual transport direction. The Williams Formation indicates an emergence of the terrane and/or a regression of the sea as evidenced by the near-shore marginal marine sedimentary features. The rose diagram for the Schulz Ranch Member of the Williams Formation suggests a possible flu vial pattern influenced by tidal fluctuation. The source for many of the Upper Cretaceous sediments was probably from a major u p lift to the east of the Santa Ana Mountains (Popenoe, 1973). Limited paleocurrent data from these Upper Creta- 30 CGOus strata suggest a sediment transport direction to the southeast. The Pal eocene is represented by the Silverado Formation which strongly suggests a very nearshore to continental environment. The presence of lig n itic sediments and p is o litic sandy clays give evidence of either lagoonal or lacustrine environments. Field obser vations in Modjeska Canyon suggest a bar-beach restricted zone with evidence of rip-up clasts and load features. Paleocurrent data from Paleocene sediments show a northwesterly transport direction. The rose diagram for the Silverado Formation implies a possible flu vial pattern affected by longshore currents. A slight inundation of the sea or a minor u p lift of the terrane took place during Eocene time and is represented by the sediments of the Santiago Formation. Near shore marginal marine environments prevailed during this time. Data values plotted on the rose diagram for the Santiago Formation suggest a flu v ia l-d e lta ic environment. Eocene paleocurrent data suggest a west-northwest direction of sediment transport. 31 CONCLUSIONS An interpretation of the paleogeography and depositional environments of the Santa Ana Mountains from the Upper Cretaceous to the Eocene was made from the study of paleocurrent data and fie ld ob servations of sedimentary structures. The Upper Cretaceous series shows the development of a marine basin of deposition beginning with the vertical gradation of continental conglomerates to a near-shore marginal environment. A gradual encroachment of the sea or a subsidence of the terrane allowed the deposition of sediments in outer shelf to bathyal waters. As the Cretaceous came to a close the sea withdrew and once again sedimenta tion occurred in near-shore shallow marine environments. Limited paleocurrent data from the Upper Cretaceous indicate a sediment trans port direction to the southeast. During Paleocene time, marginal marine to continental sedi mentation suggests a further withdrawal of the sea or an emergence of the terrane. Coal beds are observed and indicate a lagoonal or lacus trine environment. Paleocurrent analysis indicates sediment transport to the northwest. Near-shore marginal marine sediments typify the sediments of the Eocene in the area of the Santa Ana Mountains. A west-north- westerly direction of sediment transport is indicated from paleo current studies. 32 REFERENCES 33 REFERENCES Allen, J. R. L ., 1963, The classification of cross-stratified units, with notes on th eir origin: Sedimentology, v. 2, p. 93-114. Allison, E. C ., 1970, Basement rocks of the northern Santa Ana Moung'ii/? tains: jjn Geologic Guidebook, Southeastern Rim of the Los Angeles Basin, Orange County, C alifornia, Pacific Section, AAPG-SEPM-SEG, Los Angeles, p. 33-36. Almgren, A. A., 1973, Upper Cretaceous foramifera in southern C alifor nia: jji Cretaceous Stratigraphy of the Santa Monica Mountains and Sirrii H ills , southern C alifornia, Pacific Section S.E.P.M., Los Angeles, p. 31-44. California Division of Mines and Geology, 1966 (third printing, 1976), Geologic map of C alifornia, Santa Ana sheet, Sacramento, California. Chayes, F ., 1954, Discussion: Effect of change of origin on mean and variance of two-dimensional fabrics: Am . Jour. S ci., v. 252, p. 567-570. Colburn, I. P., 1970, Paleogeographic implications of the Cretaceous beds in the Santa Ana Mountains, California: iji Geologic Guide book, Southeastern Rim of the Los Angeles Basin, Orange County, C alifornia, Pacific Section A.A.P.G.-S.E.P.M.-S.E.G., Los Angeles, p. 31-32. Compton, R. R., 1967, Manual of Field Geology, 4th ed., John Wiley and Sons, New York, N.Y., 378 p. Curray, J. R ., 1956, The analysis of two dimensional orientation data: Jour. Geology, v. 64, p. 117-131. Dickerson, R. E ., 1914, The Martinez and Tejon Eocene and associated formations of the Santa Ana Mountains: Univ. C alif. Pub., Dept. Geol. Sci. B u ll., v. 8, no. 11, p. 257-274. Donn, W . L. and Shimer, J. A ., 1958, Graphic Methods in Structural Geology, Appleton-Century-Crofts, In c., New York, N.Y., 180 p. Dott, R. H., J r ., 1953, Dynamics of subaqueous gravity depositional processes: Am . Assoc. Petroleum Geologists Bull: v. 47, p. 104- 128. 34 Fisher, D. J ., 1938, Problem of two t i l t s and the stereographic pro jection: Am . Assoc. Petroleum Geologists B u ll., v. 22, no. 9, p. 1261-1271. Howell, D. G ., 1975’, Middle Eocene paleogeography of southern C alifor nia: iji Weaver, D. W., Hornaday, G. R ., and Tipton, A., (eds.), Paleogene Symposium and Selected Technical Papers, Pacific Section, A.A.P.G.-S.E.P.M.-S.E.G. conference on future energy horizons of the Pacific Coast, Long Beach, C alifornia, p. 272-293. Howell, D. G .; Stuart, C. J .; P la tt, J. P. and H ill, D. J ., 1974, Pos sible s trik e -s lip faulting in the southern California borderland: Geology, v. 2, no. 2, p. 93-98. Jizba, Z. V ., 1953, Mean and Standard deviation of certain geological data: a discussion: Am . Jour. S c i., v. 251, p. 899-906. Klein, G. deV., 1967, Paleocurrent analysis in relation to modern marine sediment dispersal patterns: Am . Assoc. Petroleum Geolo gists B u ll., V. 51, no. 3, p. 366-382. Link, M. H ., 1975, M a tilija sandstone: a transition from deep-water turbidite to shallow-marine deposition in the Eocene of California: Jour. Sed. Petrology, v. 45, no. 1, p. 63-78. Merschat, W . R ., 1971, Lower Tertiary paleocurrent trends, Santa Cruz Island, California: unpub. M. S. thesis: Ohio Univ., Athens, Ohio, 77 p. Middleton, G. V. and Hampton, M. A., 1973, Sediment gravity flows: mechanics of flow and deposition: i_ n Turbidites and Deep Water Sedimentation, Pacific Section S.E.P.M. Short Course, Anaheim, p. 1-38. Popenoe, W . P., 1936, The upper Cretaceous stratigraphy and paleonto logy of the northern Santa Ana Mountains: unpub. Ph. D. disserta tion, C alif. Inst, of Tech., 162 p. ________ 1942, Upper Cretaceous formations and faunas of southern California: Am . Assoc. Petroleum Geologists B u ll., v. 26, no. 2, p. 162-187. 1973, Southern California Cretaceous formations and faunas with special reference to the Si m i H ills and Santa Monica Moun tains: iji Cretaceous Stratigraphy of the Santa Monica Mountains and Simi H ills , southern California, Pacific Section, S.E.P.M., Los Angeles, p. 15-29. 35 Popenoe, W . P., Imlay, R. W., and Murphy, M. A., 1960, Corrélation of the Cretaceous formations of the Pacific Coast (United States and northwestern Mexico): Geol. Soc. America B u ll., v. 71, p. 1491- 1540. Popenoe, W . P., and Woodring, W . P., 1945, Paleocene and Eocene s tr a ti graphy of northwestern Santa Ana Mountains, Orange County, C ali fornia: U.S. Geol. Survey Oil and Gas Inv. Prelim, chart 12. Potter, P. E. and Pettijohn, F. J ., 1963, Paleocurrents and Basin Analysis, Academic Press In c., New York, 296 p. Reed, R. D. and H o llis te r, J. S., 1936, Structural evolution of southern California: Am . Assoc. Petroleum Geologists Pub., 157 p. Roth, J. C ., 1958, Geology of a portion of the southern Santa Ana Mountains, Orange County, California: unpub. M. A. thesis, Univ. C a lif., Los Angeles, 92 p. Sage, 0 ., 1973, Paleocene geography of southern California: unpub. Ph.D. dissertation, Santa Barbara, Univ. C alifornia, Santa Barbara, 250 p. Sage, 0 ., J r ., 1973, Paleocene geography of the Los Angeles region: in Kovach, R. L ., and Nur, A., (eds. ) , Proceedings of the Con ference on tectonic problems of the San Andreas fa u lt system, Stanford Univ. Pubs. Geol. S c i., v. 13, p. 348-357. Stauffer, P. H ., 1967, Grain flow deposits and th eir implications, Santa Ynez Mountains, California: Jour. Sed. Petrology, v. 37, no. 2, p. 487-508. Stevenson, R. E ., 1948, The Cretaceous stratigraphy of the southern Santa Ana Mountains, California: unpub. M. A. thesis, Univ. C a lif., Los Angeles, 37 p. Tanner, W . F ., 1955, Paleogeographic reconstructions from cross-bedding studies: Am . Assoc. Petroleum Geologists B u ll., v. 39, no. 12, p. 2471-2483. Walker, R. G. and M utti, E ., 1973, Turbidite facies and facies asso ciations: iji Turbidites and Deep Water Sedimentation, Pacific Section S.E.P.M. Short Course, Anaheim, p. 119-158. Wbodford, A. 0 ., McCulloch, T. H ., and Schoel1hamer, 1972, Paleogeo graphic significance of metatuff boulders in middle Tertiary strata, Santa Ana Mountains, California: Geol. Soc. America B u ll., V. 83, p. 3433-3436. Yeats, R. S., 1968, Rifting and Rafting in the southern California Borderland: _ T n Dickenson, W . R ., and Grantz, A ., (eds. ), Pro ceedings on conference on geologic problems of San Andreas Fault systems, Stanford Univ. Pubs. Geol. S c i., v. 11, p. 307-322. Yeats, R. S ., Cole, M. R ., Merschat, W . R. and Parsley, R. M., 1974, Poway fan and submarine cone and r iftin g of the inner southern California Borderland: Geol. Soc. America B u ll., v. 85, p. 293-1 302. Yerkes, R. F ., McCulloh, T. H ., Schoel1hamer, J. E ., and Vetter, J. G. 1965, Geology of the Los Angeles Basin, California -- an in tro duction: U. S. Geol. Survey Prof. Paper 420-A, 57 p. ,37 APPENDICES Appendix 1. S tatistical data showing paleocurrent directions by class frequency, vector and arithmetic mean, consistency ratio and vector magnitude. Each division on the rose diagram equals one data value, unless noted otherwise. 39" STATISTICAL ANALYSIS FOR FORMATION: KLH GROUPING: Group 1 Loc. 8 CLASS 0 - 30 31 - 60 61 - 90 9 1 - 1 2 0 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY 0 0 4 4 0 0 1 0 2 1 0 0 M EA N 105 143.8 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 90.0 81.0 Group 1 Holz Shale Member Ladd Formation Upper Cretaceous Series 301 W 2 70 90 E 2 4 0 8100 6568 12.0 39.44% 4.73 40 STATISTICAL ANALYSIS FOR FORMATION: Kws GROUPING: Gr 2 Loc 2 ,3 ,5 ,7 ,8 ,1 0 CLASS 0 - 30 4 31 - 60 0 61 - 90 0 91 - 120 2 121 - 150 4 151 - 180 1 181 - 210 4 211 - 240 3 241 - 270 1 271 - 300 1 301 - 330 2 331 - 360 2 TYPE VECTOR ARITHMETIC CLASS FREQUENCY M EA N 197.4 180.9 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 103.1 102.8 Group 2 Schulz Ranch Member Williams Formation Upper Cretaceous Series 300 240 10628 10568 24 13.5% 3.23 90 E 41 STATISTICAL ANALYSIS FO R FORMATION: Silverado (Tsi) GROUPING: All Tsi Localities CLASS CLASS FREQUENCY 0 - 30 16 31 - 60 2 61 - 90 2 9 1 - 1 2 0 3 121 - 150 2 151 - 180 5 181 - 210 211 - 240 241 - 270 0 7 6 300 W 2 7 0 -H 271 - 300 7 240 301 - 330 . 9 331 - 360 26 TYPE M EAN S S^ VECTOR 334.8 73.0 5337 ARITHMETIC 221.8 112.4 12631 NO. O F DATA POINTS 85 CONSISTENCY RATIO (L) 48 .32% VECTOR MAGNITUDE (R) 41 .1 Silverado Formation (a ll groups) Paleocene Series Each division equals two data values. '42 STATISTICAL ANALYSIS FOR FORMATION: Tsi GROUPING: Gr 1, Loc 21,23,24 CLASS 0 - 30 31 - 60 61 - 90 91 - 120 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY 11 2 1 1 0 1 0 0 3 3 8 22 M EAN 344.3 236.8 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 47.3 111.1 Group 1 S ilverado Formation Paleocene Series W 2 7 0 2 4 0 2235.7 12348 52 75.9% 39.5 Each division equals two data values. 43 STATISTICAL ANALYSIS FO R FORMATION: Tsi GROUPING: Gr 2, Loc 14,16,17 CLASS 0 - 3 0 3 31 - 60 0 61 - 90 0 9 1 - 1 2 0 0 121 - 150 0 151 - 180 1 181 - 210 0 211 - 240 3 241 - 270 1 271 - 300 1 301 - 330 0 331 - 360 1 TYPE VECTOR ARITHMETIC CLASS FREQUENCY M EA N 283.3 176.5 NO. O F DATA POINTS CONSISTENCY RATIO (L) ,VECTOR MAGNITUDE (R) 77.5 121 Group 2 Silverado Formation Pal eocene Series 2 40 6003 14640 10 33.7% 3.4 9 0 E STATISTICAL ANALYSIS FOR FORMATION: Tsi GROUPING: Gr 3, Loc 27 CLASS 0 - 30 31 - 60 61 - 90 91 - 120 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY M EA N 165.0 205.3 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 108.7 96.4 Silverado Formation Pal eocene Series 11701 9300 3.0 33.3% 1.0 45 STATISTICAL ANALYSIS FOR FORMATION: Tsi GROUPING: Gr 4, Loc 6,7 CLASS 0 - 30 31 - 60 61 - 90 9 1 - 1 2 0 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY M EA N 278.8 232.0 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 63.3 85.6 Group 4 S ilverado Formation Pal eocene Series 300 W 2 7 0 2 4 0 4006 7330 6.0 56.4% 3.4 46 STATISTICAL FORMATION: GROUPING: ANALYSIS FO R Tsi Gr 5, Loc 4,11 CLASS CLASS FREQUENCY 0 - 30 1 3 1 - 6 0 0 61 - 90 1 9 1 - 1 2 0 2 121 - 150 1 151 - 180 1 181 - 210 211 - 240 241 - 270 0 0 0 300 W 2 7 0 -W 271 - 300 0 2 40 301 - 330 0 331 - 360 0 TYPE M EA N S sZ VECTOR 103.2 52 2682 ARITHMETIC 100.8 51.7 2671 NO. O F DATA POINTS 6. 0 CONSISTENCY RATIO (L) 70. 58% VECTOR MAGNITUDE (R) 4, 23 Group 5 S ilverado Formation Pal eocene Series %1 STATISTICAL ANALYSIS FOR FORMATION: Tsi GROUPING: Gr 6, Loc 13 CLASS 0 - 3 0 0 31 - 60 0 61 - 90 0 9 1 - 1 2 0 0 121 - 150 0 151 - 180 1 181 - 210 0 211 - 240 2 241 - 270 1 271 - 300 2 301 - 330 0 331 - 360 2 TYPE VECTOR ARITHMETIC CLASS FREQUENCY M EA N 267.6 269.9 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 62.0 62.1 Group 6 S ilverado Formation Paleocene Series 3843 3856 8.0 57.2% 4.57 ■is STATISTICAL ANALYSIS FOR FORMATION: Santiago (Tsa) GROUPING: A ll Tsa L o c a litie s CLASS 0 - 30 31 - 60 61 - 90 9 1 - 1 2 0 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY 8 6 7 4 13 5 6 10 17 14 22 8 M EA N 286.2 211.9 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 89.9 97.4 Santiago Formation (a ll groups) Eocene Series 79925 9495 120.0 25.0% 30.0 .49 STATISTICAL ANALYSIS FO R FORMATION: Tsa GROUPING: Gr 1, Loc 1,22,25,26 CLASS 0 - 3 0 31 - 60 61 - 90 9 1 - 1 2 0 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY M EAN 343.7 187.4 NO. O F DATA POINTS CONSISTENCY RATIO (L) IVECTOR MAGNITUDE (R) 87.5 115.4 Group 1 Santiago Formation Eocene Series 3 30 30C 30 W 2 7 0 - 2 4 0 ' 210 150 180 S 7654 13371 41 24.6% 10.1 -50 STATISTICAL ANALYSIS FO R FORMATION: Tsa GROUPING: Gr 2, Loc 9,12,18 CLASS 0 - 30 31 - 60 61 - 90 91 - 120 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY M EA N 279.8 254.6 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 64.0 69.1 Group 2 Santiago Formation Eocene Series 300 90 E 2 4 0 4100 4774 39.0 56.3% 21 .9 STATISTICAL ANALYSIS FOR FORMATION: Tsa GROUPING: Gr 3, Loc 13, 19, 20 CLASS 0 - 30 31 - 60 61 - 90 9 1 - 1 2 0 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY M EAN 174.0 191 .3 NO. O F DATA POINTS CONSISTENCY RATIO (L) VECTOR MAGNITUDE (R) 78.2 76.2 Group 3 Santiago Formation Eocene Series W 2 7 0 6142 5811 18 43.8% 7.9 90 E 52 STATISTICAL ANALYSIS FOR FORMATION: GROUPING: CLASS 0 - 3 0 31 - 60 61 - 90 9 1 - 1 2 0 121 - 150 151 - 180 181 - 210 211 - 240 241 - 270 271 - 300 301 - 330 331 - 360 TYPE VECTOR ARITHMETIC CLASS FREQUENCY 3 1 2 0 0 3 0 3 4 0 4 2 M EA N 298.8 198.8 NO. O F DATA POINTS CONSISTENCY RATIO (L) .VECTOR MAGNITUDE (R) 84.2 111 .8 Group 4 Santiago Formation Eocene Series 7088 12489 22 26.66% 5.86 53 Appendix 2. Paleocurrent measurements, listed by formation and locality. Primary sedimentary structures are identified. :54 HOLZ SHALE MEMBER - G R O U P 1 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY fO CÜ -a O J c O J s- o S87°W S75*E S68°E S87°W S87°E N87°E N80°E N82°W N65*E N80°E S15°W S85°E *NOTi: - THESE D A TA POINTS W E R E ROTATED AT THE OUTCROP SCHULZ RANCH MEMBER - G R O U P 2 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY: x-bed S76°W,25° S55°W,35° S20°W,14° 61.0 2 1 x-bed S76°W,25° S85°W,28° N47°W,05° 7.6 3 x-bed S76°W,25° S62°W,24° S30°E,06° 7.6 3 x-bed S76°W,25° N88°W,27° N22°W,11° 7.6 3 x-bed S76°W,25° S66°W,35° S45°W,11° 7.6 3 x-bed S70°W,33° S50°W,30° S44°E,11° 5.1 5 x-bed S70°W,33° S48°W,34° S16°W,15° 10.2 5 parting 1ineation S70°W,33° S55°E,40° S74°E,64° 5 x-bed S70°W,33° N40°W,31° N13°E,35° 61.0 5 x-bed S50°W,25° S25°W,38° S06°E,18° 30.5 7 x-bed S50°W,25° S15°W,27° S49°E,15° 12.7 7 x-bed S50°W,25° S45°W,35° S32°W,09° 15.2 7 x-bed S50°W,25° S40°W,25° S45°E,04° 10.2 7 x-bed S85°W,35° S80°W,24° S85°E,11° 30.5 8 x-bed S85°W,35° N30°W,32° N27°E,35° 5.1 8 x-bed S85°W,35° N60°W,29° N27°E,19° 15.2 8 pebble- fille d channel S60°W 30.5 8 x-bed S85°W,35° N75°W,33° N13°E,11° 5.1 8 x-bed S85°W,35° S90°W,44° N74°W,10° 2.5 8 x-bed S68°W,23° S60°W,25° S06°W,04° 10.2 10 36 SCHULZ RANCH MEMBER - G R O U P 2 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed x-bed x-bed x-bed S68°W,23° S68°W,23° S68°W,23° S68°W,23° S50°W,33° S50°W,37° N80°W,35° S77°W,40° N11°W,29° S27°W,17° N45°W,19° S87°W,I8° 10.2 7.6 63.5 7.6 10 10 10 10 !57 SILVERADO FORMATION - G RO UP 1 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed S63°W,26° N72°W,42° N39°W,29° 12.7 21 x-bed S63°W,26° N68°W,4I° N08°W,32° 15.2 21 x-bed S63°W,26° N87°W,37° N48°W,I9° 10.2 21 x-bed S63°W,26° N87°W,34° N41°W,17° 12.7 21 x-bed S63°W,26° N6S°W,3Sf N22%,27° 15.2 21 x-bed S63°W,26° N67°W,37° N27°W,27° 10.2 21 ; x-bed S63°W,26° N64°W,29° N10°W,24° 15.2 21 x-bed S63°W,26° N76°W,28° NI4°W,16° 10.2 21 x-bed S63°W,26° N70°W,30° NI6°W,22° 15.2 21 x-bed S63°W,26° N55°W,51° N3I°W,43° 12.7 21 x-bed S63°W,26° N70°W,30° NI6°W,22° 12.7 21 x-bed S63°W,26° N90°W,30° N32°W,43° 12.7 21 x-bed S63°W,26° N66°W,27° N06°W,22° 15.2 21 x-bed S63°W,26° N75°W,20° N12°E,17° 10.2 21 x-bed S63°W,26° N65°W,36° N23°W,28° 12.7 21 x-bed S63°W,26° S85°W,31° N42°W,I2° 15.2 21 x-bed S63°W,26° N90°W,26° NI5°W,I2° 5.1 21 x-bed S63°W,26° N85°W,22° N04°E,I3° 10.2 21 x-bed S63°W,26° NI0°W,30° N20°E,44° 3.8 21 x-bed S63°W,26° N35°W,26° N11°E,33° 2.5 21 x-bed S63°W,26° N50°W,41° N18°W,38° 5.1 21 58' SILVERADO FORMATION - GROUP I PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed S63°W,26° N45°W,38° NI0°W,38° 2.5 21 X”bed S63°W,26° N35°W,57° N18°W,57° 3.8 21 x-bed S63°W,26° N50°W,4I° N18°W,38° 5.1 21 • x-bed S63°W,26° N70°W,33° N22°W,24° 12.7 21 x-bed S63°W,26° N50°W,33° N08°W,32° 7.6 21 x-bed S63°W,26° N35°W,46° NI0°W,48° 2.5 21 x-bed S63°W,26° N75°W,36° N33°W,23° 5.1 21 x-bed S63°W,26° N85?W,29? N24°W,15° 10.2 21 x-bed S63°W,26° N40°W,25° N10°E,3I° 3.8 21 x-bed S63°W,26° N35°W,52° NI5°W,53° 2.5 21 x-bed S63°W,26° N30°W,46° N06°W,50° 10.2 21 x-bed S63°W,26° NI5°W,37° NI1°E,48° 25.4 21 x-bed S63°W,26° N30°W,33° N05°E,40° 10.2 21 x-bed N63°W,11° N05°W,33° NI2°E,29° 10.2 23 x-bed N63°W,n° N00°W,29° N2I°E,26° 7.6 23 x^bed N52°E,I5° N03°W,27° N35°W,22° 30.5 24 x-bed N52°E,I5° N34°E,I7° N25°W,05° 7.6 24 x-bed N52°E,I5° N80°E,I5° S24°E,07° 5.1 24 ' x-bed N52°E,15° N39°E,27° NI2°E,07° 15.2 24 1 x-bed N52°E,15° N30°E,29° N11°E,16° 20.3 24 x-bed N52°E,I5° N40°W,25° N69°W,29° 15.2 24 59 SILVERADO FORMATION - G R O U P 1 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed x-bed x-bed x-bed x-bed x-bed x-bed x-bed x-bed x-bed N52°E,15° N52°E,15° N52°E,15° N52°E,15° N52°E,15° N52°E,15° N52°E,15° N52°E,15° N52°E,15° N52°E,15° S85°W,19° N82°W,28° N18°W,20° N39°W,12° N10°E,26° N48°E,25° N66°E,26° N40°E,41° N75°E,31° S85°W,25° S71°W,33° S84°W,40° N60°W,20° N89°W,19° N22°W,18° N42°E,10° N85°E,11° N34°E,26° S88°E,18° S73°W,36° 8.9 15.2 25.4 20.3 15.2 2.5 2.5 61.0 15.2 7.6 24 24 24 24 24 24 24 24 24 24 60 SILVERADO FORMATION - G RO UP 2 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed x-bed x-bed x-bed x-bed x-bed x-bed x-bed x-bed x-bed N15°E,55° N15°E,55° N15°E,55° N15°E,55° N45°E,33° N45°E,33° N84°E,21° N84°E,21° N84°E,21° N84°E,21° N07°W,32° N02°E,44° N30°W,37° N12°W,27° N80°E,27° N28°E,45° N70°W,32° N47°E,32° N65°E,27° N73°E,23° S41°W,27° S52°W,15° S61°W,36° S37°W,33° Sn°E,18° N04°W,16° N79°W,52^" N10°E,19%" N23°E,1%7 N15°E,05° ' 15.2 7.6 30.5 25.4 7.6 38.1 22.9 30.5 22.9 14 14 14 14 16 16 17 17 17 17 61 SILVERADO FORMATION - G RO UP 3 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed x-bed x-bed S04°W,29° S04°W,29° S04?W,29° S57°W,20° S05°E,39° S10°E,41° N41°W,23° S27°E,11° S36°E,14° 12.7 15.2 12.7 27 27 27 62' SILVERADO FORMATION - G RO UP 4 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed x-bed x-bed x-bed x-bed x-bed S65°W,20° S65°W,20° S65°W,20° S65°W,20° S65°W,20° S70°W,25° N80°W,51° S08°W,55° S60°W,40° S50°W,42° S70°W,18° N70°W,28° N66°W,36° S86°W,36° S56°W,20° S39°W,23° N38°E,03° N11°W,18° 20.3 15.2 10.2 7.6 7.6 30.5 63 SILVERADO FORMATION - G RO UP 5 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed x-bed x-bed x-bed x-bed scour channel S60°W,25° S60°W,25° S60°W,25° S60°W,25° S60°W,25° S60°W,25° N85°W S30°E,22° N74°E,3>° S20°W,33° S10°W,31° S35°W,20° N26°E,15° S76°E,33° N69°E,59° S26°E,21° S39°E,24° S69°E,11° 91.4 182.8 305.0 152.0 152.0 30.5 4 4 4 4 4 11 64 SILVERADO FORMATION - G RO UP 6 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed x-bed x-bed x-bed x-bed x-bed S72°W,26° S72°W,26° S72°W,26° S72°W,26° S72°W,26° S72°W,26° N80°W,25° S60°W,35° S85°W,39° S80°W,30° S34°W,36° S72°W,34° Norw ,12° S33°W,11° N74°W,15° N61°W,05° S08°E,22° S72°W,34° 61.0 76.0 30.5 91 .4 61.0 61.0 13 13 13 13 13 13 SANTIAGO FORMATION - G ROUP 1 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY scour N85°W 20.3 1 channel x-bed N48°E,26° N37°E,I9° S74°W,08° 15.2 22 x-bed N48°E,26° N65°E,28° S49°E,08° 7.6 22 x-bed N48°E,26° N50°E,28° N73°E,02° 15.2 22 x-bed N7I°E,23° N75°E,28° S39°E,12° 10.2 22 x-bed N71°E,23° N20°W,32° N52°W,39° 25.4 22 x-bed N71°E,23° N3I°W,25° N65°W,37° 30.5 22 x-bed N7I°E,23° N25°W,23° N65°W,34° 25.4 22 x-bed N71°E,23° N08°W,20° N6I°W,27° 61 .0 22 x-bed N71°E,23° N09°W,26° N52°W,31° 38.1 22 x-bed N71°E,23° N20°W,13° N79°W,26° 30.5 22 x-bed N71°E,23° N07°W,37° N37°W,38° 61 .0 22 x-bed N7I°E,23° N03°W,33° N39°W,34° 2.5 22 x-bed N71°E,23° N20°E,22° N46°W,18° 20.3 22 x-bed N71°E,23° N55°E,15° N83°W,09° 15.2 22 x-bed N71°E,23° N30°E,42° N03°E,28° 15.2 22 1 x-bed N71°E,23° N03°E,30° N39°W,29° 30.5 22 x-bed N71°E,23° N17°E,25° N39°W,21° 45.7 22 x-bed ' S52°E,06° N83°E,28° N74°E,24° 63.5 25 x-bed S52°E,06° N60°E,28° N49°E,26° 7.6 25 x-bed S52°E,06° N58°E,38° N50°E,36° 12.7 25 66 SANTIAGO FORMATION - G RO UP 1 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed S52°E,06° N05°W,15° N18°W,20° 10.2 25 x-bed S52°E,06° N44°E,07° N01°E,09° 15.2 25 x-bed S52°E,06° N85°W,06° N69°W,12° 15.2 25 x-bed S52°E,06° N57°E,34° N48°E,32° 10.2 25 x-bed S52°E,06° S40°E,15° S32°E,09° 15.2 25 x-bed S-52°E,06° N25°W,09° N36°W,15° 7.6 25 x-bed S52°E,06° S60°W,16° S74°W,18° 30.5 25 x-bed S52°E,06° S30°W,23° S44°W,23° 10.2 25 x-bed S52°E,06° N30°W,13° N05°E,32° 5.1 25 x-bed S52°E.06° N14°E,29° N37°W,19° 10.2 25 x-bed S52°E.06° N73°E,21° S40°E,05° 5.1 25 x-bed S40°W,34° S04°W,32° S71°E,T9° 7.6 26 x-bed S40°W,34° S34°W,28° N65°E,07° 10.2 26 x-bed S40°W,34° S20°E,30° S83°E,31° 30.5 26 x-bed S40°W,34° N30°W,22° N11°E,46° 76.2 26 x-bed S40°W.34° S35°W,35° S33°E,03° 50.8 26 x-bed S40°W,34° N25°W,16° N18°E,43° 30.5 26 x-bed S40°W,34° S12°W,35° S70°E,29° 38.1 26 x-bed S40°W,34° S35°W,38° S02°W,05° 76.0 .26 x-bed S40°W,34° S28°W,35° S47°E,07° 61.0 26 67 SANTIAGO FORMATION - G RO UP 2 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed S54°W,13° S75°W,21° N78°W,10° 7.6 9 x-bed S54°W,13* S65°W,25° S76°W,12° 7.6 9 x-bed S54°W,13° S85°W,27° N73°W,17° 7.6 9 x-bed S 54:% # ÿ' N85°W,34° N67°W,25° 20.3 9 x-bed S54°W,13° S40°W,20° S18°W,08° 15.2 9 x-bed S54°W,T3° S55°W,10° N51°E,03° 15.2 9 x-bed S54°W,13° S75°W,44° S82°W,32° 15.2 9 x-bed S54°W,13° S90°WJ8° N45°W,n° 182.8 9 bounce cast S85°W 9 x-bed S54°W,13° N87°W,23° N56°W,15° 22.9 9 x-bed S54°W,13° N90°W,22° N58°W,14° 30.5 9 x-bed S54°W,13° N60°W,25° N31°W,23° 27.9 9 x-bed S54°WJ3° S75°W,33° S86°W,21° 5.1 9 x-bed S54°W,13° S60°W,31° S64°W,18° 10.2 9 x-bed S05°W,52° S25°W,39° N36°W,19° 52.4 12 x-bed S05°W,52° S30°W,47° N62°W,20° 91 .4 12 x-bed S05°W,52° S59°W,69° N89°W,49° 30.5 12 x-bed S05°W,52* S65°W,62° N78°W,50° 106.6 12 x-bed S05°W,52° S50°W,49° N66°W,34° 30.5 12 x-bed S05°W,52° S30°W,52° S77°W,23° 30.5 12 x-bed S05°W,52° S20°W,86° S31°W,37° 30.5 12 ______ 68 SANTIAGO FORMATION - G RO UP 2 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DTP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed S05°W,52° S23°W,71° S50°W 25° 5.1 12 x-bed S45°W,40° S03°E,48° S50°E 34° 15.2 12 x-bed S55°W,23° S58°W,19° N41°E 04° 7.6 18 x-bed S55°W,23° S45°W,36° S30°W 14° 7.6 18 x-bed S55°W,23° S70°W,33° N83°W 12° 15.2 18 x-bed S55°W,23° S43°W,24° S29°E 05° 12.7 18 x-bed S55°W,23° S70°W,26° N54°W 07° 30.5 18 x-bed S55°W,23° S43°W,24° S29°E 05° 12.7 18 x-bed S55°W,23° S70°W,2ê° N54°W 07° 30.5 18 x-bed S55°W,23° S74°W,20° N03°W 08° 22.9 18 x-bed S55°W,23° S68°W,34° N90°W 13° 7.6 18 x-bed S55°W,23° S55°W,31° S55°W 08° • 10.2 18 x-bed S55°W,23° S35°W,27° S19°E 09° 17.8 18 x-bed S55°W,23° N10°W,10° N36°E 29° 7.6 18 x-bed S55°W,23° N85°W,19° Norw 15° 22.9 18 x-bed S55°W,23° S57°W,34° S61°W 11° 61 .0 18 x-bed S55°W,23° S85°W,27° N38°W 13° 25.4 18 x-bed S55°W,23° S87°W,28° N40°W 14° 7.6 18 x-bed S55°W,23° S68°W,35° S89°W 13° 10.2 18 x-bed S55°W,23° S78°W,28° N51°W 11° 12.7 18 69 SANTIAGO FORMATION - G ROUP 3 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed S80°W,26° S50°W,34° S04°W,17° 17.8 13 x-bed S80°W,26° S60°W,52° S46°W,29° 7.6 13 x-bed S82°W,13° S37°E,24° S56°E,32° 30.5 19 x-bed S82°W,13° S27°E,26° S47°E,32° 45.7 19 x-bed S82°W,13° S80°W,43° S79°W,30° 30.5 19 x-bed S82°W,13° N45°W,25° N15°W,20° 12.7 19 ^ S82°W,13° S37°W,27° sn°w,20° 38.1 19 x-bed S82°W,13° S74°W,34° S70°W,21° 61.0-91.4 19 x-bed S82°W,13° S53°W,23° S26°W,13° 30.5 19 x-bed S82°W,13° S70°W,27° S60°W,15° 30.5 19 x-bed S87°W,27° S55°W,22° S38°E,14° 15.2 20 x-bed S87°W,27° N36°E,19° N65°E,41° 30.5 20 x-bed S87°W,27° S50°W,12° S70°E,19° 30.5 20 x-bed S87°W,27° S75°W,33° S37°É,08° 20.3 20 x-bed S87°W,27° N65°W,33° N14°W,T5° 7.6 20 x-bed S87°W,27° S60°W,19° S52°E,13° 7.6 20 x-bed S87°W,27° S40°W,19° S47°E,19° 7.6 20 X-bed S87°W,27° S65°W,23° S36°E,10° 7.6 20 70 SANTIAGO FORMATION - G RO UP 4 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed N75°W,10° N30°W,39° N30°W,39° 15.2 28 x-bed N75°W,10° S65°W,33° S65°W,33° 76.2 31 x-bed N75°W,10° S65°W,14° S65°W,14° 30.5 31 scour channel N75°W,10° N78°E,25° N78°E,25° 30.5 31 scour channel N75°W,10° N55°E,32° N55°E,32° 38.1 31 scour channel N75°W,10° N71°E,33° N71°E,33° 91 .4 31 x-bed N75°W,10° N08°E,12° N08°E;12° 30.5 31 x-bed N75°W,10° N01°E,24° N01°E,24° 30.5 31 x-bed N75°W,10° N25°W,15° N25°W,15° 30.5 31 x-bed N75°W,10° N17°W,18° N17°W,18° 61 .0 31 scour channel N75°W,10° N30°E ------ 32 x-bed N75°W,10° S62°W,08° S62°W,08° 30.5 32 x-bed N75°W,10° S54°W,17° S54°W,17° 30.5 32 x-bed N75°W,10° S25°E,04° S25°E,04° 30.5 32 x-bed N75°W,10° N35°W,27° N35°W,27° 30.5 32 x-bed N75°W,10° S60°W,23° S60°W,23° 91 .4 32 x-bed N75°W,10° N42°W,08° N42°W,08° 76.2 32 x-bed N75°W,10° S78°W,12° S78°W,T2° 61 .0 32 X-bed N75°W,10° S35°W,09° S35°W,09° 91 .4 32 x-bed N75°W,10° S17°E,11° S17°E,11° 122.0 32 •71 SANTIAGO FORMATION - G RO UP 4 PRIMARY SEDIMENTARY STRUCTURE REGIONAL MAXIMUM DIP AZIMUTH ORIGINAL FEATURE MAXIMUM DIP AZIMUTH CORRECTED FEATURE MAXIMUM DIP AZIMUTH THICKNESS (cm) LOCALITY x-bed x-bed N75°W,10° N75°W,10° S05°E,24° N52°W,22° S05°E,24° N52°W,22° 45.7 30.5 32 32 \ 72 Appendix 3. Computer program for rotation (tw o -tilt). 73 ’EP WRRJG.TILT.FORT' ’EP WRRJG.TILT.FORT' 00010 00020 00030 000Ü0 00050 00060 00070 00080 00090 001 00 00110 00 120 00130 00140 00 15 0 00160 0 017 0 00 180 00190 00200 00210 00220 00230 00240 00250 00260 00270 00280 00290 00300 00310 00320 00330 00340 00350 00360 00370 00380 00390 00400 004 10 00420 00430 00440 00450 00460 00470 00480 00490 00500 00510 00520 00530 00540 00550 00560 00570 00580 00590 00600 00610 00620 00630 C T W 0 T I L T 4-03-78 FOR GEOLOGY GROUP, SJOGREN, BREA RES. C TO CALCULATE CORRECTED AZIMUTH AND DIP OF CROSS-BEDDING READS ANGLE AND DIP FOR FORMATION AND CROSS-BED FROM FILE FT05. EACH GROUP OF DATA HAS ONE CARD WITH TITLE, THEN DATA CARDS -- AZIMUTH ANGLE IS IN COLS. 4-7 FOR FORMATION, COLS. 23-26 FOR X-BEDS. DIP IN DEGREES IS IN COLS. 14-15 AND 34-36, RESPECTIVELY. AZIMUTH FORMAT IS ’N##W’, WHERE N IS N/S, ## IS ANGLE, W IS W/E. OPTIONAL AZIMUTH INPUT IS IN FORMAT ’ ###' AS DEGREES IN SAME COLS. PUT ' 1' IN COL.20 FOR 'OVERTURNED' BEDS, ( FLOPS CORR. AZI. OVER.) BLANK DATA CARD = PRINT AVERAGE AZIMUTH OF GROUP, READ NEXT NAME. IF FIRST AZIMUTH = NEG. , AVERAGE AS ABOVE, THEN PRINT PLOT. ( CALLS SUBR. 'TWOPLT', FOR GOULD PLOT - INCLUDE 'TWOGLD' ) INTEGER »2 IC0LM(200), ILIN0(200) DIMENSION NAME(18), IC0M(6), SECTR(25) 5 F0RMAT(18A4) 10 FORMAT( 3X ,A1 ,F2 .0 ,A1 ,6X ,F2 .0 ,4X ,11 ,2X , A 1 , F2 . 0 , A 1 ,7X , F3 .0 , A 5X , 7A4) 20 FORMAT( ’ 1' ,33X,'TWOTILT PROBLEM COMPUTATION'//,20X,l8A4,///, 1 18X ,'F 0 R M A T I 0 N',15X,’C ROSS BED S'//, 4IX, 1'0 B S E R V E D C O R R E C T E D' ,//,18X , ’DIP AZIMUTH DIP’ 2 , 5X, 'DIP AZIMUTH DIP DIP AZIMUTH DIP',/) 30 FORMAT(19X ,A1 ,F4 .0 , 'DEG ’ , A 1 , F6 . 0 ,1X , A 1 ,4X , A 1 , F4 . 0 , ' DEG ',A1,F6.0) 40 FORMAT( '+ ' ,T64 ,A 1 ,F4 .0 , 'DEG ',A1,F6.0) 50 FORMAT(/20X ,A4 ,6a4) 60 FORMAT( / 52X,'AVG. PH1= ' , T64 , A 1 , F4 . 0 , ' DEG ',A1,F6.0/) 70 FORMAT( ’1' ,//l8X ,3( 'DIP AZIMUTH DIP’,5X)/) DATA QNORTH ,SOUTH,EAST,WEST /'N' ,'S ' , 'E ' , 'W'/, ZERO/'O'/ X , lAST/'*'/, BLANK /' EQUIVALENCE ( IBLNK, BLANK ) '/, SECTR /25*0./ 99 SUMSIN=0. SUMCOS=0. AD = 1.74533 *.0 1 AD90 = AD * 90. ADI 80 = AD *180. READ AND WRITE FIRST TITLE CARD KS W=0 NPTS = 0 READ(5 ,5 ,END=2000) NAME write(6,20) name KNT=6 AL1 = 0. C----- READ AND UNSCRAMBLE INPUT DATA 10 0 READ(5 ,10 ,END=80 DQNS ,AL1 ,QEW,BE1 ,1OV R , FN S , AL 2 , FE W , BE 2 ,1 COMP ,ICOM IF(KNT.EQ.6) WRITE(6,50) ICOMP,ICOM C TEST FOR SUMMARY PRINTOUT = BLANK CARD OR AL1 = -1 IF(IC0MP.NE.IBLNK.AND.KNT.NE.6) go to 850 IF( AL1+BE1+AL2+BE2 .LE. 0.) GO TO 800 102 KNT=KNT+1 IF(MOD(KNT ,50) .EQ .0) WRITE(6,70) IND=IBLNK IF(IOVR.GT.O) IND=IAST TEST MODE OF INPUT - QMODE = ZERO IF( QNS .NE QUADRANT OR ABSOLUTE DEGREES IF( QEW .LE. IF( QEW .EQ. IF( FEW .LE. WRITE(6 ,30) 104 WRITE(6,105) 105 FORMAT( ’ ***** GO TO 100 .OR. AND . BLANK ZERO BLANK.AND . BLANK.AND. FNS FE W AL 1 AL2 . NE.BLANK .LE. ZERO .EQ. 0. .EQ. 0. GO TO GO TO GO TO GO TO 1 10 106 1 06 106 QNS ,AL1 ,QEW,BE1 ,IND , FNS ,AL2 ,FE W,BE2 INCORRECT AZIMUTH DATA’ ) 74 00640 00650 00660 00670 00680 00690 00700 00710 00720 00730 00740 00750 00760 00770 00780 00790 00800 0 0810 00820 00830 00840 00850 00860 00870 00880 00890 00900 009 1 0 00920 00930 00940 00950 009 60 00970 00980 00990 0 1000 0 10 10 0 1020 0 1030 0 1040 0 1050 0 1060 0 1070 0 1080 0 1 090 0 1100 0 1110 0 1120 0 1130 0 1140 0 1150 0 1160 0 1170 0 1180 0 1190 0 1200 0 12 10 0 1 220 0 1230 0 1240 01250 106 1 10 1 15 1 20 130 200 210 220 230 GENERATE AZIMUTH ANGLE IN ABSOLUTE DEGREES CALL BCNV( QEW, API, 202, 1,0) CALL BCNV( FEW, AP2, 202, 1,0) IF( AL1 .NE. 0.) API = API + 10.* AL1 IF( AL2 .NE. 0.) AP2 = AP2 + 10.* AL2 AL1 = API AL2 = AP2 QEW = BLANK FEW = BLANK QMODE = BLANK WRITE(6,30) QNS ,AL1 ,QEW,BE1 ,IND , FNS , AL2 ,FEW,EE2 IF( QMODE .EQ. BLANK ) GO TO 300 . GENERATE AZIMUTH ANGLE FROM QUADRANT INPUT DATA IF( QNS .EQ. SOUTH ) GO TO 120 IF( QNS .NE. QNORTH) GO TO 104 IF( QEW .EQ. EAST ) GO TO 115 IF( QEW .NE. WEST ) GO TO 104 AP1=(360.-AL1) GO TO 200 AP1 = AL1 GO TO 200 IF( QEW .EQ IF( QEW .NE AP1=(180.+AL1) GO TO 200 AP1=(180.-AL1) IF( FNS. EQ. SOUTH) GO TO 220 IF( FNS .NE.QNORTH) GO TO 104 IF( FEW .EQ. EAST ) GO TO 210 IF( FEW .NE. WEST ) GO TO 104 AP2=(360.-AL2) GO TO 300 AP2=AL2 GO TO 300 IF( FEW .EQ. EAST ) GO TO 230 IF( FEW .NE. WEST ) GO TO 104 AP2=(180.+AL2) GO TO 300 AP2=(180.-AL2) EAST ) GO TO 130 WEST ) GO TO 104 300 306 310 330 -- TEST FOR SIMPLE CASES - AZIMUTHS THE SAME ? REVERSE AZIMUTH IF X-BED DIP > 90. IF( BE2 .LE. 90.) GO TO 310 IF( BE2 .GT. 180.) WRITE(6,306) FORMAT( 20X,’ ERROR ?, X-BED DIP > 180.') BE2 = 180. - BE2 AP2 = AP2 + 180. IF( AP2 .GT. 360.) AP2 = AP2 - 360. IF(AP1.NE.AP2) GO TO 330 PHI = API IF( BEI .GT. BE2 ) PHI = PHI +180. GAM = ABS( BE1-BE2 ) IF( PHI .GT. 360.) PHI = PHI -360. GO TO 700 AZIMUTHS DIRECTLY OPPOSED ? IF(ABS(AP1-AP2).NE.180.) GO TO 340 PHI = AP2 GAM = BEI + BE2 IF( GAM .LE. 90.) GO TO 700 PHI = PHI + 180. GAM = 180. - GAM 0 1250 0 1270 0 1280 0 1290 0 1300 0 1310 0 1 320 0 1 330 0 1340 0 1350 0 1360 0 1 370 0 1380 0 1 390 0 1400 0 14 10 0 1420 0 1430 0 1440 0 1450 0 1460 0 1470 0 1480 0 1490 0 1500 0 15 10 0 1520 0 1530 0 1540 0 1550 0 1560 0 1570 0 1580 0 1590 0 1600 0 16 10 0 16 20 0 16 30 0 16 40 0 16 50 0 1660 0 1670 0 1680 0 1690 0 1700 0 1710 0 1720 0 17 30 0 17 40 0 1750 0 1760 0 1770 0 1780 0 1790 0 1800 0 18 10 0 1820 0 1830 0 18 40 0 1850 0 1860 0 1870 IF( PHI .GT. 360.) PHI = PHI -360. GO TO 700 CHECK FOR ZERO DIPS ? 340 IF(BE1 .NE .0 . ) GO TO 350 PHI=AP2 GAM=BE2 GO TO 700 350 IF(BE2 .NE.O.) GO TO 360 PHI = AP1 +180. IF( PHI .GT. 360.) PHI = PHI -360. GAM = BEI GO TO 700 VERTICAL CROSS-BED DIP ANGLE ? 360 IF( BE2 .NE. 90. ) GO TO 380 PHI = AMOD( AP1+180.,360.) GAM = 90. - BEI GO TO 700 X 1 ,Y1 , X2 ,Y2 . . . EXCEPTIONS ACCOUNTED FOR, COMPUTE 380 CONTINUE A1 = API *AD A2 = AP2 *AD XI = SIN( A1 ) Y1 = COS( A1 ) X2 = SIN( A2 ) Y2 = COS( A2 ) CALC X,Y,Z FOR UNIT VECTOR NORMAL TO CROSS BED PLANE ( SINN IS POSITIVE ABOVE HORIZ. PLANE ) CB2 = COS( BE2*AD ) SB2 = SIN( BE2*AD ) SINN = CB2 COSN = SB2 XN = X2 * COSN YN = Y2 * COSN DELTA = ANGLE BETWEEN FORMATION AZIMUTH AND X-BED AZIMUTH DELTA = AP2 - API IF( DELTA .LT. 0.) DELTA = DELTA + 360. CALC ( XR,YR ) = PROJECTION OF POINT ’N* ON FORMATION STRIKE DELSN = SIN( DELTA «AD ) * COSN A90 = A1 + AD90 XR = SIN( A90 ) * DELSN YR = COS( A90 ) « DELSN . . . FIND DISTANCE ’R-N' AND ANGLE OF LINE R-N FROM VERTICAL ( ANGLE ARN IS < 0. FOR DELTA > 270. OR < 90. ) XYR2 = XR*XR + YR*YR DRN2 = 1. - XYR2 DRN = SQRT( DRN2 ) ARN = ARCOSC SINN / DRN ) IF( DELTA .LT. 90. .OR. DELTA X ARN = - ARN . . . ROTATE TO 'ARNC', FIND ARNC = ARN + BE1*AD RHO = DRN * SIN( ARNC ) FIND AZIMUTH OF ROTATED DEL2 = ARCOSC SQRT( XYR2 GT. 270. ) RHO' = HORIZ. DIST. TO FORM. STRIKE R IF( DELTA .GT. 180.) DEL2 IF( ARNC .LT. 0. ) DEL2 DEL2 = DEL2 + 90. IF( lOVR .GT. 0 ) PHI = API + DEL2 IF( ARNC .LE. AD90 ) GO TO 420 PHI = PHI + 180. X-BEDS AND CHECK SENSE OF ARNC / ( XYR2 + RHO«RHO ) ) ) / AD = 180. - DEL2 = - DEL2 DEL2 = - DEL2 76 0 18 80 0 1890 0 1900 0 19 10 0 1920 0 1930 0 19 40 0 19 50 0 I960 0 1970 0 1980 0 1990 02000 020 10 02020 02030 02040 02050 02060 02070 02080 02090 02100 02110 02120 02130 02 140 02150 02160 02170 0 2 18 0 02190 02200 02210 02220 02230 02240 02250 02260 02270 02280 02290 02300 02310 02320 02330 02340 02350 02360 02370 0 2380 02390 02400 024 10 02420 0 2430 02440 02450 0 2 4 6 0 02470 0 2480 02490 420 PHI = AMOD( PHI+360., 360.) . . . CALC CORRECTED X-BED DIP 'GAM' BY COS( G ) = ZC ZC = DRN » ABS( COS( ARNC ) ) GAM = ARCOSC ZC ) / AD 700 7 10 720 7 30 -- PRINT AZIMUTH IN SAME FORMAT AS INPUT DATA A1 = SINC PHI*AD ) B1 = cose PHI»AD ) SUMSIN = SUMSIN +A1 SUMCOS = SUMCOS +B1 PHIO = PHI IFC QMODE .EQ. BLANK ) GO TO 750 PRINT AZIMUTH AS 'N##W IFCPHI.GT.180.) GO TO 720 IFCPHI.GT.90.) GO TO 710 FNSzQNORTH FEW=EAST GO TO 750 FNS=SOUTH FEW=EAST PHIO=180.-PHI GO TO 750 IFCPHI.GT.270.) GO TO 730 FNS=S0UTH FE W= WEST PHIO=PHI-180. GO TO 750 FNS=QNORTH FEW= WEST PHIOr 360.-PHI 750 WRITEC6.40) FNS,PHIO,FEW,GAM ADD DATA TO COL, LINE & SECTOR ARRAYS FOR LATER PLOT IFC GAM .GT. 40.) GAM = 40. NPTS = NPTS + 1 I = PHI / 15. + 1.999 IFC I .EQ. 1 ) 1 = 2 SECTRCI) = SECTRCI) + 1. IFC NPTS .GE. 200 ) GO TO 100 ICOLMCNPTS) = 41.5 + A1 * GAM ILINOCNPTS) = 25.4 -.6* B1* GAM GO TO 100 ------ PRINT SUMMARY 800 KSW=1 GO TO 900 8 01 KSW=3 GO TO 900 850 KSW=2 FEWSAV = FEW FNSSAVrFNS - AVERAGE AZIMUTH ANGLE IN THIS GROUP 900 PHIO = 90. IFC SUMCOS EQ. 0.) GO TO 904 PHIO = ATANC SUMSIN/SUMCOS ) / AD FORMAT OUTPUT AZIMUTH SAME AS INPUT MODE 904 PHI = PHIO IFC PHIO .LT. 0.) PHIO = PHIO + 180. IFC SUMSIN .LT. 0.) PHIO = PHIO + 180. IFC QMODE .NE. BLANK ) GO TO 910 77 0 2500 025 10 02520 02530 02540 02550 02560 02570 02580 02590 02600 0 26 10 0 26 20 02630 02640 02650 02660 02670 0 26 80 02690 027 00 027 10 027 20 027 30 027 40 027 50 02760 02770 02780 02790 02800 028 1 0 02820 02830 028 40 028 50 02860 0 2870 02880 02890 02900 029 1 0 02920 02930 02940 029 50 0 2960 02970 029 80 02990 03000 03010 0 3020 0 3030 0 3040 0 3050 0 3060 03070 0 3080 03090 03100 03110 PHI = PHIO GO TO 920 C 910 PHI = ABS( PHI ) F E W= WE S T IF(SUMSIN.GT,0.) FEW=EAST FNS=S0UTH IFCSUMCOS.GT.O.) FNS=QNORTH C PRINT AVERAGE AZIMUTH 920 WRITE(6,60) FNS, PHI, FEW KNT=KNT+1 IF(M0D(KNT,50).EQ.O) WRITE(6,70) KNT=KNT+1 IF(MOD(KNT,50).EQ.O) WRITE(6,7 0) KNT=KNT+1 IF(M0D(KNT,50).EQ.O) WRITE(6,7 0) SUMSINzO. SUMCOS=0. C TEST FOR PRINTER-PLOT ? IF( AL1 .EQ. 0.) GO TO 1400 SECTRC1) = AL1 C . . . CALL SUBR. FOR PLOT ON PRINTER OR GOULD CALL TWOPLTC NAME, NPTS, PHIO, ICOLM, ILINO, SECTR ) C C------- SEQUENCE CONTROL FOR NEXT ACTION 1400 NPTS = 0 DO 1410 I = 1, 25 1410 SECTRCI) = 0. AL1 = 0. GO TO C 99 , 1 500 ,2000) ,KSW C . . . PRINT NAME FOR NEXT DATA SECTION 1500 WRITEC6,50) IC0MP,IC0M FNS=FNSSAV FEW=FEWSAV KS W=0 NPTS = 0 GO TO 102 C C . . . CALL SUBR. TO END PLOTING 2000 NPTS = 0 CALL TWOPLTC NAME, NPTS, PHIO, ICOLM, ILINO, SECTR ) RETURN END C--------- T WO PLT --------- SUBR. CALLED FROM TWOTILT PROGRAM C 04-03-78 VERSION TO PLOT POINTS ON PRINTER - SJOGREN, BREA SUBROUTINE TWOPLTC NAME, NPTS, PHIO, ICOLM, ILINO, SECTR ) C DIMENSION NAMEC18), IC0LMC200), ILIN0C200), SECTRC25) INTEGER *2 ICOLM, ILINO, ISECTR, LINEC81), IB ,IAST , I ONE,NINE DATA IB/' '/, lAST/'*'/, lONE /'I'/, NINE/'9'/ IFC NPTS .EQ. 0 ) GO TO 400 Q_______ for PRINTER PLOT OF AZIMUTH AND DIP ANGLES WRITEC6,16) NAME, NPTS, PHIO 16 FORMATC'1',// 20X,'DATA PLOT FOR: ’, 18A4, // 20X, X ’NUMBER OF DATA POINTS =', 15,' AVERAGE AZIMUTH = '» X F4.0,' DEG / 24X,'C CIRCLE IS DRAWN AT 37 DEGREES ) ) IFC NPTS .EQ. 0 ) GO TO 400 IFC NPTS .LT. 200 ) GO TO 22 19 FORMATC*24X, 'C ONLY FIRST 200 DATA POINTS SHOWN BELOW )') NPTS = 200 78 03120 03130 03140 03150 03160 03170 0 3180 03190 03200 03210 03220 0 3230 03240 03250 03260 03270 03280 03290 03300 0 3310 03320 03330 03340 03350 03360 03370 03380 03390 03400 034 10 0 3420 03430 0 3440 03450 0 3460 03470 03480 0 3490 03500 03510 03520 0 3530 03540 03550 READY 22 26 C . . 50 55 C 140 C . . 150 170 180 186 400 SET UP LINE COUNTER FOR MAIN PRINT LOOP LINAT = 1 WRITE(6 ,26) FORMATC /// ) START OF LOOP -- SET LINE TO BLANKS DO 5 5 I = 1, 81 LINECI) = IB TEST IF 37 DEGREE CIRCLE NEEDS INSERTING IFC LINAT .LT.4 .OR. LINAT .GT.46 ) GO TO 150 IFC LINAT .EQ.4 .OR. LINAT .EQ.46 ) GO TO 140 CALCULATE COL. POSITIONS FOR AT 37 DEGREE DIP A1 = 36.4* SINC ARCOSC C25.-LINAT)/21.0 ) ) I = 4 1.4 + A1 LINECI) .= lAST I = 41.4 - A1 LINECI) = lAST IFC LINAT .EQ. 25 ) LINEC41) = lAST GO TO 150 STRING OF '*’ AT VERY TOP AND BOTTOM OF CIRCLE LINEC39) = lAST LINEC41) = lAST LINEC43) = lAST LOOP TO INSERT MARKS FOR DATA POINTS DO 180 I = 1 , NPTS IFC ILINOCi) .NE. LINAT ) GO TO 180 N = ICOLMC I ) IFC LINECN) .GE. IB ) GO TO 170 ALREADY A MARK - INCREMENT DIGIT UNTIL '9' IFC LINECN) .NE. NINE ) LINEC N ) = LINEC N ) GO TO 180 FIRST MARK IN COLUMN LINEC N ) = lONE CONTINUE PRINT THIS ROW OF PLOT WRITEC6 ,186) LINE FORMATC 10X, 81A1 ) LINAT = LINAT + 1 IFC LINAT .LE. 50 ) GO TO 50 END OF PRINTER PLOT RETURN END 256 Appendix{4. Vector mean program and input instructions. 80 TAPE CTBXBO.OATA NEW START TAPE DIMENSION ICKHEMC4),NCLASC12)*RSI NEC15),RC0S(15),NTITLE(12) INTEGER S0UTH,EAST,WEST,OIRCTl,DIRCT2,UPPER PRS§ DATA NORTH,SOUTH,EAST, WEST/ 'N^, •■S', 'E’, 'W •/ DATA NCLAS,SIGN/1 2+0,0.0/ DATA X,IB,SUM,ICXHEM/0.0,1,0.0,4+0/ DATA RSINE/.259, .707, .966, .966, .707,.259,-.259,-.707,-.966,-.966; 1 -.707,-.259/ DATA RC0S/.966,.707,.259,-.259,-.707,-.966,-.966,-.707,-.259 2 , .259, .707, .966/ DATA IC,VAR2,AVAR2,V,W,AZL0,AZHI/1,0.0,0.0,0.0,0.0,0.0,0.0/ PI = 3 .14159265 READ(7,77)NTITLE WRITEC6,77)NTITLE 77 F0RMATC1X,12A4) 10 READC7,100,END=110) DIRCT1,DEGRE1,DIRCT2 100 F0RMATCA1 ,1X,F3 .0,1 X,A1 ) C.... CONVERT from QUADRANTS TO AZIMUTHS. IFCDIRCTl .EQ. SOUTH) GO TO 20 IFCDIRCT2 .EQ. WEST) DEGREl = 360. - DEGREl G0 TO 30 20 IF(DIRCT2 .EQ. WEST) DEGREl = 180. + DEGREl IFCDIRCT2 .EQ. EAST) DEGREl = ISO. - DEGREl 30 SUM = SUM + DEGREl X = X + 1 . IFCAZLO .GT. DEGREl) AZL3 =DEGRE1 IFCAZHI .LT. DEGREl) AZHI =OEGREl lA = 0 40 lA =IA +1 IFC DEGREl .GT. CFL0ATClA)+30.0))GO TO 40 NCLASCIA) = NCLASCIA) + 1 GO TO 10 110 AMEAN = SUM/X DO 49 1=1,12 IFCABSCFL0ATC3O+I -15)-AMEAN) .GT. 180.) GO TO 48 AVAR2 = AVAR2 + CNCLASCI) + CCFLOATC30+I-15)-AMEAN)++2)) GO TO 49 48 DIFF=180. - CABSCFL0ATC30+I-15)-AMEAN) -180.) AVAR2 = AVAR2 + CNCLASCI) +CDIFF++2)) 49 CONTINUE AVAR2 = AVAR2/CX-1.0) AVAR = SQRFCAVAR2) WRITEC6,1000) 112 FORMATCIH ,T10, ’ARIIHMETIC MEAN MAY BE IN ERROR.*/ 2 T10,'DATA POINTS DIVERGE .GT. 180 DEG.*) WRITEC6,101) AMEAN,AVAR,AVAR2,X IFCCAZHI -AZLO) .GT. 180.0)WRITEC6,112) WRITEC5,1000) 101 FORMAT Cl HO,F6, 'ARITHMETIC*,T20, 'STD DEV ',T30, 'VARIANCE',T43, 2 '-NO. OF ’, / ,T8, 'MEAN ',T22, ' C S ) ' , T3 1 , * C S ++2 ) ' , T42, 'DATA PTS . *, /, 3T8,F6.1,T21,F6.1,T31,F9.2,T42,F6.1) DO 50 I =1,12 V=V + CNCLASCI) * RC0SCD) 50 w = W + CNCLASCI) * RSINECD) VMEAN = W/V DO 90 1=1,6 ICKHEMCl) = ICKHEMCl) +NCLASCI) 90 ICKHEMC2) = ICKHEMC2) + NCLASCI+6) DO 91 1=1,3 IC K H E M C 4 ) = I C K H E M C 4 ) ♦ N C L A S C I ) ♦ N C L A S C I + 9 ) 91 IC K H E M C 3 ) = I C K H E M C 3 ) + N C L A S C I + 3 ) + N C L A S C I + 6 ) 81- 92 irCICKHEMCI) .GT. ICKHEM(IB)) IB = IFCVMEAN .LT. 0.0) SIGN = 1.0 ANGLE = ATANCVMEAN) +180./PI GO TO C6l,62,63,64),IB 61 VMEAN = C180.+SIGN) + ANGLE GO TO 65 62 VMEAN = C180.+CSIGN+1.0)) + ANGLE GO TO 65 63 VMEAN = 180.0 + ANGLE GO TO 65 64 VMEAN =(360.0 * SIGN) + ANGLE 65 R = SQRTCCV+*2)+CW++2)) XL = CR/X)+100.0 D0 60 I =1,12 IFCABS (FLOATC30+I-15)-VMEAN) .GT. 180.)GO TO 70 VAR2 = VAR2 + (NCLAS(I) +<<FLOAT<30+1-15)-VMEAN)++2)) GO TO 60 70 DIFF = 180. - CCABSCCFL0ATC30+I-15)-VMEAN))-180 .)) VAR2 = VAR2 + CNCLASCI) +CDIFF++2)) 60 CONTINUE VAR2 = VAR2/CX-1 .0) VAR = S3RTCVAR2) WRITEC6,105)VMEAN,R,XL,VAR2,VAR 105 F0RMATC1HO,3X, 'VECTOR MEAN’,2X, *R VALUE',2X,'L VALUE’,3X, ’S ++2 2 ,3X, ’STO DEV */T 8, F6 .1 , T1 7, F 6 .2 , T2 7, F6 .2 , T3 4 , F8 .1 , T 4 7, F6 .2 ) WR ITEC6,1000 ) WRITEC6,106) 106 FORMATC1 HO,T11 , 'LOWER CLASS’,T31, 'UPPER CLASS',T52, 'CLASS' 2 /,T13, 'LIMITS *,T33, "LIMITS", T50, 'FREQUENCY *,/, 3T10,*CIN DEGREES) ',T30, ' CIN DEGREES)*) DO 80 I =1,12 UPPER = 30+1 LOWER = C30+CI-1)) +1 80 WRITEC6,108) LOWER,UPPER,NCLASCI) 108 FORMATCIH ,T15,13,T35,I 3,T50,I 3) 1000 FORMATCIX,/) STOP END READY 82j VECTOR M EAN PROGRAM This program provides the following statistical parameters. (1 (2 (3 (4 (5 (6 (7 (8 Vector Mean Varience and Standard Deviation of the data from the vector mean. Arithmetic Mean. Variance and Standard Deviation of the data from the arithmetic mean. Class frequency for 12 classes (30 degrees interval). Total number of data points processed. Resultant Vector Magnitude (R). Consistency Ratio (L) 100 percent =; perfectly consistent alignment of data points 0 percent = no Consistency of alignment. INPUT INPUT CARD IMAGE COLUMNCOLUMNCOLUMNCOLUMNCOLUMNCOLUMNCOL 0 0 0 0 00 0 00 11 1 11 1 11 1 12 1 2 3 4 5 6 7 8 9 0 1;2 3 4 5 6 7 8 9 0 X * # # . * v Where: x = N (north) or S (south) # # = Degree measure (0°-90°) y = E (east) or W (west) * = Blank . = Decimal point The program converts quadrant readings to azimuth for statistical processing. 83

Linked assets

University of Southern California Dissertations and Theses

Conceptually similar

PDF

Magnetostratigraphy of Upper Cretaceous strata in the Santa Ana Mountains, Southern California

PDF

The foraminifera of the Cook's Mountain Eocene of Texas

PDF

The physical and magnetic polarity stratigraphy of the upper Cretaceous - lower Tertiary North Horn and Flagstaff Formations, Gunnison Plateau, central Utah

PDF

Quaternary stratigraphy and sedimentation of the Santa Monica Shelf, Southern California

PDF

Crustal and upper mantle structure of Mainland China

PDF

The mode and environment of deposition of a late Cretaceous resedimented conglomerate, near Reef Ridge, Kings County, California

PDF

Foraminiferal biostratigraphy of the Anita Formation, Western Santa Ynez Mountains, Santa Barbara County, California

PDF

Clay mineralogy of the North Bering Sea Shallows

PDF

The structural geology of the Swansea area east-central Buckskin Mountains Yuma County, Arizona

PDF

Pliocene ostracoda from Southern California

PDF

Structural geology of the central portion of the Highland Spring Range, Clark County, Nevada

PDF

Petrologic studies in the basement of the upper plate of the Whipple detachment fault, Whipple Mountains, southeastern California

PDF

Paleomagnetic analysis of Eocene rocks from the Peninsular Ranges Terrane, San Diego, California

PDF

Seismotectonics of the Santa Monica and Palos Verdes fault systems in the Santa Monica Bay, Southern California

PDF

Application of discriminant function analysis to geologic problems

PDF

Petrology of Jurassic plutons and older crystalline units, the Cargo Muchacho Mountains, southeastern California

PDF

Geology of the southwesternmost Whipple Mountains, San Bernandino County, California

PDF

The Eocene sequence of central Reef Ridge: Sedimentary structures and mode of deposition of Avenal Sandstone and significance of the sandy units of the Kreyenhagen Shale

PDF

Suspended sediment over Redondo submarine canyon and vicinity, southern California

PDF

Geochemistry and diagenesis of Santa Barbara Basin sediments off southern California

Asset Metadata

Creator Davis, Robert Allen (author)

Core Title Paleocurrent analysis of the Upper Cretaceous, Paleocene and Eocene strata, Santa Ana Mountains, California

Degree Master of Science

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

Tag Earth Sciences,OAI-PMH Harvest

Format application/pdf (imt)

Language English

Contributor Digitized by ProQuest (provenance)

Permanent Link (DOI) https://doi.org/10.25549/usctheses-c37-382918

Unique identifier UC11657608

Identifier EP58638.pdf (filename),usctheses-c37-382918 (legacy record id)

Legacy Identifier EP58638.pdf

Dmrecord 382918

Document Type Thesis

Format application/pdf (imt)

Rights Davis, Robert Allen

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