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1.1 Geography 486/586 Splansky and Laris 2005 PALOS VERDES PENINSULA I. HISTORY

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1.1 Geography 486/586 Splansky and Laris 2005 PALOS VERDES PENINSULA I. HISTORY 1.1 Geography 486/586 Splansky and Laris 2005 PALOS VERDES PENINSULA I. HISTORY: DATES AND PLACE NAMES In 1602 Sebastian Vizcaino, sailing northward from Acapulco, re-named the bay east of the peninsula San Pedro Bay (viewed on the Feast Day of Saint Peter). Earlier, it had been named the "Bay of Smokes" by Juan Cabrillo. Vizcaino also referred to and charted the existence of the Palos Verdes (green stalks) observed to the west of the bay. In 1784, Rancho San Pedro was granted to Juan Jose Dominguez. This change in land ownership status represented the first private land grant in Alta California and it included the Palos Verdes peninsula. Subsequent carving up of the Rancho San Pedro created one portion named Rancho de Los Palos Verdes which was acquired by the son of Juan Jose Sepulveda. In 1792, George Vancouver, on his return voyage from the Canadian Pacific coast, met and liked Father Fermin Francisco de Lasuen while visiting the Carmel Mission. Vancouver also met and liked Friar Vicente Santa Maria while visiting the San Buenaventura Mission. In 1793, while rounding the Palos Verdes peninsula, he named and charted Points Vicente and Fermin after the two clerics. II. PALOS VERDES: GENERAL TERMINOLOGY AND INFORMATION The Palos Verdes Peninsula is a northwest trending dome-like ridge, 9 miles long and up to 5 miles wide. Its crest has gentling rolling topography at elevations ranging from 1480 to 1100 feet above sea level. Below this upland, remnants of a flight of Pleistocene marine terraces ring the peninsula and demonstrate it was an island during most of its geomorphic evolution. A Simple Stratigraphy 1. Catalina Schist is metamorphic and the oldest rock on the peninsula (K/A dated to 120,000,000 BP). This rock was formed in a subduction zone and probably was not exposed to erosion until 15-16 M.Y.B.P. when it was unroofed in a submerged basin and range topographic province in the “Los Angeles Basin Inner California Borderland.” Some of the Catalina Schist material was subsequently carried northward along fault lines that mostly parallel the San Andreas Fault Zone. From late Miocene times (14.5 M.Y.B.P.), the schist formed an irregular, southwest sloping sea floor upon which sedimentary deposits were laid down and consolidated. Concurrently, igneous material was ejected to flow and harden atop the accumulating sedimentary deposits and intruded as sills into the consolidating sedimentary strata then forming atop the Catalina Schist. These sedimentary and both extrusive and intrusive igneous materials were to form the Monterey Formation. The Catalina Schist thus forms the basic core bedrock and core of the peninsula site upon which the current widely seen sedimentary and igneous materials are deposited. On the Palos Verdes Peninsula today, the Catalina Schist bedrock remains buried beneath the Monterey Formation except for one site where erosion on the northeast slope of the peninsula has stripped away overlying sedimentary materials and exposed a small section of the surface of this core bedrock. 2. The Monterey Formation is the oldest and most common sedimentary unit overlying the Catalina Schist and ranges in age from 14.5 to 3.6 M.Y.B.P. The Monterey Formation was formed by sedimentary deposition into an offshore basin floored by the Catalina Schist, accompanied by the addition of extrusive and intrusive igneous material. 1.2 Subduction Diagram Diagrams of cross sections of crustal extension 1.3 Fault and Geographic Map of onshore and offshore southern California 1.4 Large Scale map of Lithotectonic Belts 1.5 Major Faults Geomorphic Provinces 1.6 Map of LA Basin Area displaying general fault distribution, place names, etc. Strata of Palos Verdes Peninsula Diagram 1.7 Geologic Time Chart 1.8 During middle Miocene times (10-19 M.Y.B.P.), the Palos Verdes Hills area was an underwater basin that was filling with laminated diatomaceous (formed from diatoms*) mud and distal turbidites (formerly fine sediments in suspension not deposited by stream deposition) forming the base of the Monterey Formation. Subsidence of the basin kept pace with deposition and 1,000-4,900 feet of diatomaceous mud collected, while the water depth remained constant at 4,900-6,500 feet. * A diatom is any of numerous microscopic, unicellular, marine or fresh-water algae having siliceous cell walls. Diatomaceous earth contains diatoms or their fossil remains. The beginning of Pliocene time (5 M.Y.B.P.) was marked by the influx of increasing amounts of terrigenous (originating from land surface) sediment and increased rates of deposition. Through middle and late Pliocene times (3-2 M.Y.B.P.) the Palos Verdes Hills area evolved toward a shallower (3,900-4,900 feet) depositional environment. The shallowing is consistent with uplift of the peninsula which was probably underway by 3.0 .Y.B.P. The proto-Palos Verdes Hills already formed a submarine sill at least 600 feet above the surrounding sea floor. By early Pleistocene time (2 M.Y.B.P.), the sediments being deposited in the adjacent basins had coarsened and the rate of accumulation had increased to 1-2 mm per year, enough to compensate for subsidence and to produce complete filling of the Los Angeles basin by 1 M.Y.B.P. The Monterey Formation may be divided into three members; 1) The Middle Miocene Altamira Shales, 2) the late middle to early upper Miocene Volmonte Diatomite, and the 3) late upper Miocene to early Pliocene Malaga Mudstone. a) The Altamira Shales is the dominant exposed rock on the Peninsula, has an exposed thickness of 1,000 feet and contains another 1,000' concealed under the west end of the peninsula. The Altamira Shales were deposited on top of the Catalina Schist from 14.5 to 12.5 M.Y.B.P. All but the upper 150' of Altamira Shales was deposited while local submarine vulcanism occurred. The igneous activity created sills, basalt flows and numerous areas of accumulated tuffaceous material (volcanically derived ash sometimes known as tuff). The basalt sills intruded into the Altamira Shales and are irregularly exposed (they can be seen at Royal Palms County Park Beach). The Tuff has been weathered and altered and is often known as Bentonitic Tuff or Ash or Clay, or simply Bentonite. It is a distinctive unit as much as 75' thick in the lower portion of the exposed Altamira Shales (it could have been deposited from a single eruptive cycle from a submarine volcano or vent). A younger thinner bed of tuff (Miraleste Tuff) is at higher elevation. Bentonite, like all clays, organizes its molecules into flat sheets. Water molecules can slip in between these sheets and act as ball bearings. The clay can absorb a vast quantity of water thus making the clay more slippery and allowing the clay to expand in volume as much as fifteen times. The potential for mass wasting is thus much enhanced as the Bentonite beds have a shearing strength of only one-fifth to one-tenth that of other materials within the bedrock. b) The Volmonte Diatomite formation was deposited from 12.5 to 7.0 M.Y.B.P. c) The Malaga Mudstone was deposited from 7.0 to 3.5 M.Y.B.P. 3. The Monterey Formation is partly overlain by the middle to upper Pliocene Repetto Formation dominated by the Lomita Marls and Sands. These are the youngest sedimentary materials formed on the peninsula, mostly along the north and east facing lowest elevations and were deposited between about 3.0 to 2.0 M.Y.B.P. Sedimentation on this growing formation appears to have slowed or stopped between 1 and 2 million M.Y.B.P. as suggested by the absence of the Upper Pliocene and lower Pleistocene Pico Formation, which is rather thick (900- to 3,000 feet) and widespread elsewhere in the Los Angeles basin. Sedimentation resumed when the San Pedro Formation, an almost 600 feet thick sequence of fossiliferous silts, sands and gravels was deposited on the Miocene-Pliocene bedrock. This formation is younger than 700,000 Y.B.P. 1.9 III. UPLIFT AND FORMATION OF MARINE TERRACES Faulting and Uplift It has been over a century since A. C. Lawson in 1893 first recognized the importance of vertical tectonic movements in the Los Angeles Basin and the Southern California borderland. The Palos Verdes Peninsula appears to be a compressional structure resulting from vertical tectonics (uplift) along a reverse fault caught between two regional strike- slip faults. The anticlinal growth of the peninsula has long been associated with a northwest trending, southwest dipping, reverse fault. The Palos Verdes Hills are the expression of a doubly plunging anticlinorium. The emergent portion of the anticlinorium is somewhat like an iceberg as the visible part of the structure is only a fraction of its total size (9 x 5 miles and 1480’ high). Offshore stratigraphy suggests that the complete anticlinorium is at least twice as large and three times as high. Sustained anticlinal growth of the peninsula is reflected by the presence of the only exposure of basement rocks (Catalina Schist) throughout the western Los Angeles Basin, the progressive warp of originally flat-lying deposits, a sedimentary suite indicative of progressive shallowing, and the existence of a flight of emergent marine terraces.. Uplift of the Palos Verdes anticline began about 3 M.Y.B.P and has continued to the present. The end of the Pliocene has long been recognized on stratigraphic grounds to coincide with a strong compressional episode along coastal California. Recent plate tectonic reconstructions have related the onset of this compression to two distinct changes in Pacific plate motion at 2.48 and 3.4 M.Y.B.P.
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