156 CALIFORNIA COOPERATIVE OCEANIC FISHERIES INVESTIGATIONSespecially for the years 1961 and 1963) ; as upwellingceases fog also decreases, and with sunnier weatherand little turbulence a thermocline often developswhich tends to preserve a temperature gradient, Alsoduring these months, flushes of warmer oceanic waterfrom offshore may flow in on the surface of the bay.The Davidson Current period of the winter monthsis clearly indicated in Figures 1A and 1B by themarked decline in surface temperatures, the closesimilarity of average monthly maximum and minimumsurface temperatures, and the nearly uniformtemperature conditions prevailing in the upper 50meters as a result of mixing.In Figure 1C the phytoplankton volumes representmonthly averages of wet settled volumes of phytoplanktonper haul, 15 meters to the surface, taken ina 2 meter net of 173 meshes/inch. Larger diatomsand dinoflagellates are retained, but not nannoplankton.Major increases in standing crop occur in springand summer. For the 13-year period 1954-1966, maximumcrops appeared most frequently in June, butin different years peaks fell in all months fromMarch through July. Chuetoceros is usually the predominantgenus in the bay in spring and earlysummer.The most notable irregularity in the general seasonaltemperature pattern shown in Figure 1A is theunusual warm peak which occurred in February1963. This unseasonal warming, one phenomenonamong many in a winter of unusual weather, appearsin the records of shore temperatures taken along muchof the temperate Pacific coast (Scripps Institution ofOceanography, 1964). February temperatures at mostshore temperature stations in <strong>California</strong>, Oregon, andWashington exceeded temperatures recorded for thatmonth in any year through 1966 since the warm years1957-1959. In Monterey Bay this warm pulse wasaccompanied by conspicuous red tides and luminescence; the phytoplankton was dominated by Peridiwium,with lesser numbers of Ceratium and Gonyuzc-Zaz (Hopkins Marine Station, 1963). Red tides extendedat least as far north as Point Montara and insouthern <strong>California</strong> were prevalent from near SanDiego to Santa Barbara (<strong>California</strong> Marine ResourcesOperations, 1963). No unusual mortality of fishesor other marine organisms was noted, in MontereyBay or elsewhere in <strong>California</strong>, but phytoplanktonvolumes obtained in Monterey Bay rose sharply inMarch.A less compicuous warm pulse during the DavidsonCurrent period occurred in February 1961 (Figure1A) , and was reflected in shore temperatures taken atmany points along the coast (Scripps Institution ofOceanography, 1962). In contrast to the situation in1963, dinoflagellates formed less than 2% of the phytoplanktonbloom accompanying and following thewarm conditions. Instead, the phytoplankton consistedof a mixed population of diatoms characteristic ofcoastal waters ; Chaetoceros and Skeletomnza predominated,accompanied by lesser numbers of Asterionella,Thalassiosira, Nitzschia, and other forms. The characterof the phytoplankton in the March bloom of 1963suggests the growth of organisms brought in fromoceanic waters offshore, while the March bloom of1961 represents growth of resident populations characteristicof <strong>California</strong>n coastal waters.REFERENCESBolin, R. L., and D. P. Abbott. 1963. Studies on the marineclimate and phytoplankton of the central coastal area of<strong>California</strong>, 1954-1960. Calif. Coop. <strong>Oceanic</strong>. Fish. Invest.,Rept., 9 : 23-45.Calif. Marine Resources Operations. 1963. Monthly reports :February, 14 p.; hhrch, 12 p. Calif. Dept. Fish and Game,Terminal Island. (multilithed)Hopkins Marine Station. 1963. Quarterly report of the CCOFIinvestigations, Jan. 1-Mar. 31, 4 p. Stanford University,Pacific Grove. (mimeo.)Scripps Institution of Oceanography. 1962. Data report, surfacewater temperatures at shore stations, United States westcoast and Baja <strong>California</strong>, 1961. SI0 Ref., 62-<strong>11</strong> :141.Scripps Institution of Oceanography. 1964. Daily surface watertemperatures and salinities at shore stations, <strong>California</strong>,Oregon, and Washington coasts, 1963. Preliminary unofficialreport.
SEASONAL VARIATION OF TEMPERATURE AND SALINITYAT 10 METERS IN THE CALIFORNIA CURRENTRONALD J. LYNN, OceanographerBureau of Commercial Fisheries Tuna Resources laboratoryla Jolla, <strong>California</strong>INTRODUCTIONThe seasonal variation of temperature and salinityat 10 meters in the <strong>California</strong> Current is examinedfrom the <strong>CalCOFI</strong>l data record, 1950-62. The Cal-COFI station pattern off <strong>California</strong>-Baja <strong>California</strong>(Figure 1) has been occupied repeatedly since 1950.Surveys have been conducted on almost a monthlyschedule although only a portion of the station patternwas covered each time. Only four surveys wereconducted in 1961 and 1962. The sampling frequencyof salinity for 1950-62 is shown in Figure 2. At someof the stations temperature was measured a few moretimes than salinity. Harmonic curves, comprised ofthe annual and semiannual components, were fitted toeach station record by regression analysis using themethod of least squares. The harmonic curves providethe description of seasonal variation. Along with theregression analysis are descriptive statistics.The <strong>California</strong> Current SystemThe <strong>California</strong> Current is the eastern limb of theanticyclonic gyre that dominates the North PacificOcean. It is a broad sluggish current characterized bycool, low-salinity water. Warm high-salinity water isfound to the west (central North Pacific) and south(vicinity of the Gulf of <strong>California</strong>). Upwelling alongthe coastal boundary of the current introduces cool,usually high-salinity water to the surface layer. Upwellingis the process whereby the wind componentparalleling the coast (northwesterly) drives the surfacewater offshore; these waters are replaced bydeeper waters.The North Pacific gyre is largely wind-driven. Seasonalvariation of the winds is indicated by seasonalvariation of the strength and location of atmosphericpressure cells. The currents respond to variations inwind. This system was qualitatively described for the<strong>California</strong> Current region by Reid, Roden, and Wyllie(1958). A strong northerly wind component in springthrough fall strengthens the Current. In winter thenortherly component weakens or reverses and a countercurrentdevelops along portions of the coast. Theseasonal variation of the winds has a most noticeableeffect on coastal upwelling. Upwelling is strongestwhen the north and northwest winds are strongest.This situation occurs off Baja <strong>California</strong> in April andMay, off southern and central <strong>California</strong> in May andJune, off northern <strong>California</strong> in June and July, andoff Oregon in August (Reid, Roden, and Wyllie,1958).The largest and most complex changes in circulationoccur in the coastal region. A countercurrent is presentin late fall, winter, and early spring from central<strong>California</strong> to British Columbia (cf. Sverdrup, Johnson,and Fleming, 1942 ; Schwartzlose, 1963). A nearly1 <strong>California</strong> <strong>Cooperative</strong> <strong>Oceanic</strong> Fisheries Investigations.permanent eddy is found among the Channel Islandsoff southern <strong>California</strong>. The eddy is weak or nil inMarch, April, and May (Schwartzlose, 1963 ; Reid,1965). The countercurrent is usually continuousaround Point Conception in November, December, andJanuary. There is no countercurrent along northernBaja <strong>California</strong>, but major eddies do occur off southernBaja <strong>California</strong>.An atlas of sea surface dynamic topography (referencedto 500 decibars) of the <strong>CalCOFI</strong> data is underpreparation at the Scripps Institution of Oceanography(S10). The contours and gradients define thedirection and speed of the geostrophic currents.The variations of circulation and upwelling have apronounced effect on the seasonal variation of temperatureand salinity. The seasonal variation of thesecharacteristics was discussed at length by Reid,Roden, and Wyllie (1958). They gave representativecurves of the variations for diverse areas constructedfrom monthly means of <strong>CalCOFI</strong> data, 1949-55, andother sources.The following paragraphs are quoted from a reviewof the earlier work by Reid (1960, p. 81). In place ofseasonal variation curves to which his paragraphsrefer, the reader may examine similar figures of thispaper (Figures 8,10, 13 and 14).". . . Far offshore the variation, which is principallythe result of variation in radiation and exchangewith the atmosphere, has a simple pattern with thegreatest range in the highest latitude. Near the coastin the region of strong upwelling north of 34"N. theseasonal range is reduced and the cool period lengthenedby upwelling. Between 28"N. and 34"N. theupwelling occurs earlier in the year, more nearly atthe period of the offshore seasonal minimum, and increasesthe seasonal range. South of 28" N. it is thefall and winter countercurrent which accounts for thehigh range and delays the low until late spring."The seasonal variation in surface salinity . . . indicatesthat the direct eff'ect of evaporation and precipitationis small, and, indeed, there is little coherencein the variation of the northern offshore stations.Inshore it is again the processes OP upwelling in thenorth and the countercurrent in the south whichdominate the seasonal variation. The effect of thespring and summer upwelling of deeper water to thesurface in the north causes a wide range with themaximum value of salinity in summer. In the souththe winter countercurrent brings highly saline waternorthward along the coast giving a maximum inwinter. The two effects tend to cancel each other in themiddle region between 28"N. and 34"N. latitude."Recently, the seasonal variation of temperature andsalinity at diverse levels in the Point Conception(Point Arguello) region has been examined in detail(Reid, 1965).
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