Observations and Modelling of Fronts and Frontogenesis

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LIST OF TABLES Table Page 11.1 Tow start and finish positions and times 41 11.2 Winds and surface fluxes 42 11.3 Climatological sea surface temperature (°C), averaged over 150-155° W 43
OBSERVATIONS AND MODELLING OF FRONTS AND FRONTOGENESIS IN THE UPPER OCEAN I. INTRODUCTION This thesis comprises two separate projects. The common theme is fronts and frontogenesis in the upper ocean. Fronts, regions of unusually large horizontal gradients in fluid properties, are an important form of physical oceanographic variability. Though they have received considerable attention from oceanographers (the recent monograph The Physical Nature and Structure of Oceanic Fronts (Fedorov, 1986) contains 279 references), a full understanding of their role in the ocean still awaits us. In Chapter II, we present an analysis of upper ocean temperature data collected near the North Pacific Subtropical Frontal Zone. In this region of the North Pacific, the large-scale meridional gradients of temperature, salinity, and density are intensified in a Frontal Zone. Wind-driven convergence is the probable primary cause of this intensification (Roden, 1975). Many small scale fronts are evident in the data. Baroclinic instability is likely important in the development of these smaller scale features. In Chapter III, we present a model for wind-driven therniocline upwelling at a coastal boundary. In this case, the action of the wind on the ocean is again frontogenetic.
Page 1 and 2: AN ABSTRACT OF THE THESIS OF Roger
Page 3 and 4: Observations and Modelling of Front
Page 5 and 6: To my parents, Hans and Nancy Samel
Page 7 and 8: This research was supported by ONR
Page 9 and 10: TABLE OF CONTENTS I. INTRODUCTION 1
Page 11: Figure LIST OF FIGURES (continued)
Page 15 and 16: II. TOWED THERMISTOR CHAIN OBSERVAT
Page 17 and 18: oriented multiple surface fronts up
Page 19 and 20: gravity waves. A maximum of 21 and
Page 21 and 22: small, since the large-scale temper
Page 23 and 24: front at about 18.5 °C. There is f
Page 25 and 26: given in the stable cases (downward
Page 27 and 28: temperatures for January and Februa
Page 29 and 30: dominates the spectrum. At these wa
Page 31 and 32: typically iO-2iO3 °c m1-), and sin
Page 33 and 34: 11.5 Geostrophic turbulence We have
Page 35 and 36: energy of each of the longitudinal
Page 37 and 38: varying N and a flow isolated from
Page 39 and 40: adiabatic meridional displacements
Page 41 and 42: z0 34 32 V v 30 a -J 28 26 a) - 2b$
Page 43 and 44: U0 V L 0 L V 20 E 16 V 12 p ; t *,
Page 45 and 46: 30 E 50 -c a- I, 0 70 90 300 360 37
Page 47 and 48: 10 10° 10-2 1 0 -3.0 -2.0 -1.0 0.0
Page 49 and 50: 1 o 1 102 101 - 0 LU 00 x I.- - -1
Page 51 and 52: E (I) a. z 106 1 o5 102 101 100 1O
Page 53 and 54: Table 11.1 Tow start and finish pos
Page 55 and 56: Table 11.3 Climatological sea surfa
Page 57 and 58: Paulson, C. A., R. J. Baumann, L. M
Page 59 and 60: 111.1 Introduction In this chapter
Page 61 and 62: interior layers, on the horizontal
Page 63 and 64:
polynomials in z.) The vertical mom
Page 65 and 66:
hit + (hivi) = We, (8a) h2t + (h2v2
Page 67 and 68:
Equations (la) and (2a) are dynamic
Page 69 and 70:
subdivided into subdomains with dif
Page 71 and 72:
mixed layer. As is the case with (2
Page 73 and 74:
constant pressure c = 4.1x103 J K1-
Page 75 and 76:
When (28) have been solved for the
Page 77 and 78:
occur with the initial conditions w
Page 79 and 80:
analytically. Let Al2 and A23 be th
Page 81 and 82:
Shortly after t = 8.1, the mixed la
Page 83 and 84:
that around the offshore front, exc
Page 85 and 86:
the reduced equations numerically.
Page 87 and 88:
(1) The upwelled horizontal profile
Page 89 and 90:
Figure 111.1 Model geometry. zO z z
Page 91 and 92:
* j 0. -20. >\ - -40. 0 > .0 0. 40.
Page 93 and 94:
4) 20. 10. 0. 20. 1 0. 0. 0 y/X 0.
Page 95 and 96:
BIBLIOGRAPHY Batchelor, G. K. , 195
Page 97 and 98:
Rhines, P. B., 1979: Geostrophic Tu
Page 99 and 100:
APPENDIX A: DYNAMICAL DERIVATION OF
Page 101 and 102:
In a manner exactly analogous to th
Page 103 and 104:
smoothness. The large vorticities t
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